Abbe, C. , Jr . , 1899 , a General Report on the Physiography of Maryland

Home , Alcovy Mountain, Geology of Tennessee, James River Gorge, Smoke Hole Canyon, Uvala (landform), Wolfpen Ridge

Abbe , C. , Jr., 1899 , A gene ral re port on the physiography of Maryland : Maryland weather Service , p. 41-21€. Discusses physiography, landscape evolution, and drainage evolution of the Appalachians of Maryland .

Abbe , c. , Jr., 1902 , The physiography of Garrett County, Maryland, in Garrett County, Maryland: Baltimore , Maryland Geological Survey , p. 27-54. Discu�ses physiography and structural control of landforms .

Abrahams, A. D. , 1S85, Lithologic control of bedrock mea'lder dimensions in the Appalachian Valley and Ridg� province : A comment : Earth Surface Processes and Landforms, v. 10, p. 635-638. Braun's finding that the wavelength of bedrock meanders decreases as rock hardne5s increases is reconciled with Hack 's and Tinkler's finding that meander wavelength is greater in bedrock than alluvial channels. In populations of alluvial or bedrock channels, bank resistance cor.trols meander wavelength via its influence on channel shape and is negatively correlated wlth meander wavelength. In contrast, in mixed populations of alluvial and bedrock c�els, bank resistance controls meander wavelength through its effect on the recurrence interval of the channel-forming discharge and channel size and is positively correlated with meande r wavelength .

Abrahams, A. D. , and Flint, J., 1983, Geological controls on the topological properties of some trellis channel networks : Geological Society of America Bulletin, v. 94, p. 80-91. It has been assumed, but never quantitatively demonstrated, that the topological properties of trellis channel networks are strongly influenced by the unde rlying geology. In this study , the topological properties of 7 trellis networks unde rlain by a plunging syncline are analyzed and compared with those of 45 deneritic networks. The geological controls are shown to have a pronounced effect on the topological properties.

Acker, L. L. , and Hatcher, R. D., Jr., 1970, Relationships bet\�en structure and topography in northwest South Carolina: South carolina Geologic Notes, v. 14, p. 35-48 . The control of drainage orientation by joint patterns is demonstrated. Thr�e erosion surfaces are described and an example of stream capture is given.

Adams, c. C. , 1901 , Baseleveling and its faunal significance, with illustrations from the southeastern United States: American Naturalist, v. 35, p. 839- 852. Concern is with manner in which landscape evolution affects faunal distribution. Author says that the time of maxirm.un roughness in the topography coincides with greatest isolation of faunas . As base level is approached, fauna become more widely distributed . Cites examples of faunal distributions which hP believes due to shifting of divides and other landscape change;.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Adams , G. I., 1901 , Physiography and geology of the o�ark region: u. s. Geological Survey Annual Report, pt . 2, v. 2�, p. 69-94 . Pages 69-75 provide a brief description of the physiography of the Ozark region.

Adams , G. I., 1923, The formation of bauxite in sink hole&: Economic C�ology, v. 18, p. 410-412. Suggests that ba\�ite deposits result from the ac�lation and alteration of clays in sinkholes .

Adams, G. I., 1928, The course of the Ter�essee River and the physiography of the southern Appalachian region: Journal of Geology, v. 36, p. 481-493. Suggests that the lower portion of the Tennessee River acqui red its present course by extending its course over the land emerging after the Mesozoic submergence . says it made a sharp bend near Guntersville, incised its valley into the unconsolidated Cretaceous sediments, and developed its valley in adjustment to the unde rlying Faleozoic rocks as they were re-exposed. This interpretation avoids the problem of how the river was diverted across Walden Ridge .

Adams , G. I., 1956, Upland surfaces alon� the Atlantic coast of the united States, in Eighth report of the Commi ssion for the Study and Correlation of Erosion Surfaces around the Atlantic, IV, Researches in North America: Rio de Janeiro, International Geographical union, p. 22-27 . Add resses 5 basic problems : 1) How may dissected peneplains be identified? 2) Are peneplains really pediplains? 3) How may marine and estuarine terraces be identified in the Coastal Plain? 4) How may multiple erosion levels be identified in regioLs of intense deformation? 5) How may erosion surfaces be dated?

w. , Adams , H. s., and Rhoades, R. 1976, A description of vegetation on the south slopes of Peters Mountain [Abstract ): Vi rginia Journal of Science , v. 27, p. 53. Lists tree species as a function of topography and elevation.

Ahnert , F. , 1970, A comparison of theoretical slope models with slopes in ��e field: Zeitschrift fur Geomorphologie Supplementband, v. 9, p. 88-101 . Measured thickness of surficial mar.tle on gneiss hillslopes in North carolina with refraction seismograph . Found that thickness varies positively with distance from the top of the slope and r.egatively with the sine of the slope .

Alexander, w. H., 1938, The physiographic history of the Little Kanawha valley, We st Vi rginia [M.A. thesis): Cincinnati , university of Cincinatti, 48 p. Speculates on original dr�inage pattern of the Allegheny Plateau and describes geomorphic history in terms of erosion cycles. Drainage evolution is also discussed.

Ande rson, D. G. , 1970, Effects of urban development on floods in northern Virginia: U.S. Geological Survey Water-Supply Paper, v. 2001-C, 22 p. Graphical andmathemat ical relations are presented to estimate the flood-peak magnitudes having recurrence intervals ranging up to 100 years for drainage basins wi th various degrees of urban or suburban development .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Antevs , E. , !9 32, Alpine zone of Mt . Washington : Aubu rn, Maine , Me rrill & Webber, 118 p. Describes glacial history and the erfect� of frost action. Latter includes movements of debris by frost, patterned ground , solif�uction, stone streams, and planation.

Ashley, G. H, . 1930, Age of the Appalachian peneplains : Geologicdl Society of America Bulletin, v. 41, p. 695-700. Based on several lines of evidence, author argues that upl ift of the Kittatinny peneplain began no earlier than Miocene .

Ashley, G. H., 1931, Our youthful scenery: Geological Society cf America Bulletin, v. 42, p. 537-545. Argues that mountain ranges in the Appalachians all date from uplifts since the beginning of Miocene time and that all lower surfaces date from still later time .

Ashley, G.H. , 1933, The scenery of Pennsylvania, its origin and development: Pennsylvania Geological Survey , 4th series, v. G6, 91 p. Sunmarizes a number of studies by the author on landscape evolution in Pennsylvania.

Ashley, G. H. , :;35, Studies in Appalachian mountain sculpture : Geological Society of America Bulletin, v. 46, p. 1395-1436 . Concludes 1) that the present surface , though reflecting a single old peneplain, has been lowered by no-c less than 100 ft/illy since the beginning of uplift; 2) that, except near the Atlantic coast and during recent time, all the level surfaces and imaginary surfaces touching the tops of accordant hills and mountains may be accounted for by: a) local base-leveling or district base-leveling; or b) the stripping of flat-lying hard rocks;, or c) as the result of parallel lowering because of uniformity of rock and structure ; 3) that, as a rule, subsequent trenching has been the result of stream capture or other stream adjustment not associated with coastal movements; 4) that the detailed unde rlying geology must be known and taken into account if reliable conclusions about physiographic history are to be drawn; 5) that most physiographic features are much younge r than has been assumed.

Ashley, G. H., 1939, How old are the mountains?: C011100nwealth of Pennsylvania Department of Internal Affairs, v. 7-10, p. 11-16. Popular version of earlier work .

Ashley, G. H. , 1939, Mountains of Pennsylvania and their or1g1n: Commonwealth of Pennsylvania Department of Internal Affai rs, v. 8-1 , p. 8-13. Popular version of earlier work.

Ashley, G. H. , 1940, Old mountain theories are challenged by findings : C0111110nwealth of Pennsylvania Department of Internal Affairs , v. 8-2, p. 15-21 . Popular version of earlier work .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Atwood, W. w. , 1940, The physiographic provinces of North Americ.'.l: New York, Ginn and co., 536 p. Textbook with chapters on physics Jhy of Appalachians.

Baker, V. R. , 1973, Geomorphology and !l)•drology of karst drainage basins and cave channel networks in east-central New York : Water Resou�ces Research, v. 9, p. 695-706 . Free surface streams , flowing through meandering cave conduits , provide links between the upland surface catchme�ts and large karst springs draining into the major river valleys. The cave conduits fonn an integral part of a drainage organization characterized by Horton's hierarchial stream numbe rs, lengths, and drainage areas. The conduits, the highest-order streams in the hierarchy , have meandering reaches with wavelengths directly related to upstream drainage area and contributed runoff. Roth the morphology of the cave channels and the hydrology of the �arst drainage basins are strikingly similar to those observed in surface water stream systems .

Balazik, R. F. , 1967, The influence of exposure on valley morphology in western Pennsylvania [M.S. thesi�) : University Park , PA , Pennsylvania State University, 55 p. Studied relationships between valley morphology and exposure by analyzing va�iations in morphology between valleys with different orientations . Tested slope inclination, drainage basin perimeter, drainage basin area, drainage basin length, basin elongation ratio, basin circularity, stream length, drainage density, stream gradient, and stream frequency between valleys with different orientations . Found that northeast-facing slopes are steeper than southwest-facing slo�s . Stream length and frequency are greater in south-facing valleys .

Banino, G. M. , 1969, Origin of Roaring Brook : Trenton, NJ , N.J. Bureau of Geology & Topography, 8 p. Popular account of Roaring Brook , a boulder stream composed of large diabase boulders.

Bannister, E. , 1980, Joint and drainage orientation of s.w. Pennsylvania: Zeitschrift fur Geomorphology, v. 24, p. 273-286 . Correspondence between the orientation of joint and stream net works is analyzed. Joint azimuths and intensity are measured from sandstone outcrops . Orientation and length of stream reaches, delimited on topographic maps, are compared to the direction and intensity (cumulative length) of joint facets. Joint patterns dominate the orientation of streams where the relative relief and hydrostatic gradient are low. High relative relief is associated with an increase in hydraulic gradient which enables stream channels to deviate from joint-strike directions. Sou�stern Pennsylvania stream orientation is controlled by 1) joint orientation and intensity, 2) hydraulic gradient, and 3) historical drainage orientation.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Barr, T. C., 1954 , 'lhe occurrence and origin of deep pits in tt.e cumberland Plateau of Tennessee: Speleonews, Dec., p. 9-11. Considers stratigraphic position of pits a�d factors which n.ay limi t their depth.

aarr, T. C., Jr. , 1954 , Regional development of limestone caves in midd:e Tennessee: NSS Bulletin, v. 16, p. 83-90. Explains how caves may develcp in the various physiographic settings of middle Tennessee

Barr, T. C. , Jr., 1961, caves of Tennessee: Tennessee Division of Geology Bulletin, v. 64 , 567 p. Introductory section contains information about geological occurrence of caves .

Barrell, J., 1913, Piedmont terraces of the northern Appalachians and their mode of origin [Abstract ): Geological Society of America Bulletin, v. 24, p. 688-690. Uses a meL1od of projected profiles to detect marine plains that have been uplifted and largely destroyed by subaerial erosion. Argues that earlier invasion of the sea adva�ced to central Pennsylvania a� western Massachusetts

Barrell, J., 1913, Post-Jurassic history cf the northern APpalachians [Abstract]: Geological Society of America Bulletin, v. 24 , p. 690-694. Seeks to determine the age of the piedmont terraces by correlatir.g them with the strata of the Coastal Plain.

Barrell, J., 1917, Rhythms and the measurements of geologic time: Geological Society of America Bul letin, v. 28, p. 745-904 . Only parts are pertinent to geomorphology: Present rates of denudation; relations of rate to the cycle of erosion; significance of prP.sent valley forms; contrast of Cenozoic and Paleozoic continental reliefs; contrast of present and past rates of denudation.

Barrell, J., 1920, The Piedmont terraces of the northern Appalachians: American Journal of Science, v. 199, p. 227-258, 327-362 , 407-428 . A posthUIOOUs paper edited by H.H. Robinson . Includes helpful editorial comments on this and previous work of Barrell. Describes in detail the projected-profile techni que , which seems fairly objective. Barrell's explanation of the origin of the terraces is baserl on a belief in their great age and in the efficacy of marine planation.

Bascom, F. , 1921, Cycles of erosion in the Piedmont province of Pennsylvania: Journal of Geology, v. 29, p. 540-559 . Provides evidence for remnants of nine erosion surfaces - three of Cretaceous age and six of post-cretaceous age . Says could be of subaerial or marine origin. Attempts to relate these surfaces to Coastal Plain terraces.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bashore, H. B., 1896 , Notes on glacial gravels in the lower Susquehanna Valley: American Journal of Science, v. 1, p. 281--282. P.long lower Susquehanna , reports an abrupt termination of

Bassett, J. , 1976, Hydrology �•d geochemistry of the uppe r Lost River drainage basin, Indiana: NSS Bulletin, v. 38, p. 79-87 . Reports discharge and chemical measurements on sinking streams and on springs.

Beaumont , C. , Quinlan, G. M. , anrl Hamilton, J., 1987 , The Alleghanian orogeny and its relationship to the evol ution of the eastern interior, North America, in Beaumont , C. , and Tankard, A. J., eds., Sedimentary basins and basin-forming mechanisms: Canadian Society of Petroleum Geologists, Memoir 12: Canadian Soc. Petroleum Geologists, p. 425-445. From previously publi&hed work authors constructed contour map of coal burial depth (Fig. 6) (i.e., maximum previous ove rburden) in the Appalachian Plateau based on coal-moisture contents. Results �uggest that great thicknesses of Permian sedi�nts were laio ciown and subsequently eroded away. From 5,000 to 9,000 feat of rocks have been re7110Ved in the western Appalachian coal fielas, and mure in the eastern fields .

Becker, G. F., 1895, Gold fields of the southern Appalachians : u.s. Geological Survey Annual Report, v. 16, pt.3, p. 251-331. Of chief interest is p. 289-293 , where author coins �e rm "saprolite", describes saprolite, and relates it to the occurrence of placer go�.d .

Bell, A. M. , 1986, Morphology and stratigraphy of terraces in the upper �henandoah Valley, Vi•ginia [M.S. thesis]: Morgantown, wv, university of west Vi tginia, 160 p. Although relatively old deposits are preserved on carbonat�s , solution destroys terrace morpho!�- and stratigraphy. In contrast , terraces over shale bedr , retain their mrphology although they are more readily eroded away . Silty dol omite is the best compromise between these two extremes. Te rrace ..:h ronosequences adjac... Jt to thP. South Fork of the Shenandoah River exhibit at least 5 distinct morphostratigraphic units.

Benson, M. A. , 1962, Factors influencing the occurrence of floods in a humi d region of diverse terrain: u. s. Geological Survey Water-Supply Paper, v. 1580-B, p. B1-B64. Multiple- ,:�gression techniques used to determine factors . Drainage basin area most important for predjctin g flood peaks . Main channel slope next most important , and a simple yet efficient �ndex o� main-channel slope was developed . The following topographic characteristics showed little relationship to flood peaks: profile curvature, shape fac��r. altitude , stream density.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Berg, T. M. , Seven, W. D. , and Bucek, M. F., 1977, Geology and mineral resources of the Pocono Pines and Mount Pocono Quadrangles, Monroe County, Pennsylvania: Pennsylvania TOpographic and Geologic Survey, v. 204�d, 66 p. Includes short descriptions of talus , colluvium, and othP.r surficial deposits.

Berger, z. , 1978 , Stream adjustment to drop in base level tested through dynamic equilibrium and geomorphic threshold c�ncepts: A case study of some of the Allegheny' s tributaries [Ph.D. thP.sis) : Pittsburg, university of Pittsburg, 191 p. TWo groups of tributaries of the Allegheny River system were examined under the same environmental conditions but subjected to different amounts of base level drop. When the drop was greater than 105 feet, the streams cut deep valleys forming no terraces. When less than 105 feet, the vall�J exhibits 3 series of successive non--paired terraces increasing in frequency up to a point where a drop in base level is not adequate to produce and conserve terraces .

Berklan1, .J. 0., and Raymond , L. A., 1973, Pleistocene glaciation in the Blue Ridge province , southern lachian Appa MountaiTls, North Carolina : Science , v. 181, p. 651-653 . Claimed to have found glacial polish, grooves, and striations on Grandfather ��tain, North Carolina, thus suggesting Quaternary alpine glaciation . Their claims have nvt been supported.

Berry, E. W. , 1919, Upper Cretaceous floras of the eastern Gulf region in Tennessee, Mississippi , Alabama, and Georgia : U.s. Geological Survey Professional Paper, v. 112, 177 p. Has sketch re�p illustrating the distribution of streams ove r the pre-Cretaceous landscape . Thinks the Cretaceous ancestor of the Tennessee, instead of taking the sharp tum to the NW at Guntersvillt!, AL, that it does now, continued sw down either Brown or Big Spring valley and reached the sea through either Mulberry or Locust Fork of Black Wa rrior River. Local warping broke its continuity with the Bla�k Wa rrior drainage and started it toward the tM before the deposition of the Selma Chalk. The remnad:s of gravels of '1\lscaloosa age that have been traced by Wade across 'lN into KY appear to represent the gradual migration or shifting northwestward of such a stream. says there is no evidence that the Tennessee ever flowed throu

Berry, J. L., 1977, Chemical weati1ering and geomorphological processes at Coweeta, North carolina [Abstract): Geological Society of America Abstracts with Programs, v. 9, p. 120. Investigated chemical weatl�ring in residual soils on small wat.ersheds at Coweeta by analytical and petrographic means .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bethune , P., 1948, Ge0100�:phic st...dies in the Appalachians of Pennsylvanja: American Journal of Science, v. 246, p. 1-22 . Suggests that Applllachian drair.age was substantially reorganized at the time of ut>lift of the Schooley penep:ain and became superimposed frC'1111 extensive flood pl�i.ns which developed in several downwarped areas of the peneplain at the beginning of the uplift. 'lhese downwarps are recognized 1) by the convergence of northwest and southeast-flowir.g superimposed streams , and 2) by the lower level of the peneplain in these areas. Recognizes, however, ��t ridge tops have been appreciably lowered du ring the course of the present cycle. Says his findings cast doubt on the theory that the several erosion levels, such as the Harrisburg level , represent successive and temporary base levels.

Betsvn, R. P. , 1977, The hydrology of karst urban areas, in Dilamarter, R. R. , and Csallany, S. C., eds ., Hydraulic problems in karst arear-: Bowling Green, KY, Western Kentucky university Press, p. 162-175. Study of four small watersheds in Knoxville. Found that urbanization can markedly increase the yield of runoff, for under rural c�o•.ditions much of the potential runoff is lost to a soluble �:ock system. 'rtle magnitude of flooding is also increesed much more �� would occur on other areas.

Billings , w. D., and Mark, A. F. , 1957, Factors involved in the persistence of montane treeless balds: Ecoiogy, v. 38 , p. 140-142. Notes must distinguish between the problem of bald origin and bald maintenance . Balds are relative permanent because 1) treeless environment is a more severe one for seedlings; 2) most balds appear to occupy ecotonal areas near the margins of the tolerance ranges of the important regional tree species; 3) extremes of climatic cycle may completely eliminate certain tree species or at least reduce the population so that tl1e variety of available biotypes is small. A non-forested gap due to lack of a seed sourc� may then result.

Blood, P. , 1924, A profile study of erosion surfaces in Pennsylvania and Maryland [M.S. thesis] : New York, Columbia university, 32 p. By means of a study of topographic profiles, concluded that the apparent multiplicity of erosion levels can be explained on the basis of two peneplains, a higher one remnants of which may be found between 1800-2000 ft, and a lower one whose highe r remnants occur between 800-1000 ft and which includes not only the Piedmont, but also the Great Valley and Triassic Lowland .

Bloomer , R. 0., 1951 , A folded overthrust and its effect upon stream developnent in central Virginia: American Journal of Science , v. 249, p. 640-653 . A restoration of the now-eroded fault block may expl"ill the development of the subsequPnt segments of James and North rivers upstream from the west end C'lf the James River gorge at Glascow as well as the origin of Sallings Gap in Sallings Ridge . This paper i.s a good example of restoring geology by projecting contacts to a higher vertical level to see what the surface geology was like at that time, then using this to explain changes in stream courses.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Blurre, H. , and Barth, H. K., 1973 , Schichtstufenrelief und �fflachen in clen sudlichen Appa1achen-Plateaus von Tennessee (Cuestas and peneplair.s in th� southern Appalachian plateaus of Tennessee): Erda, v. 104, p. 294 313. Cuesta-landiorms of the CUmberland Plateau owe their most �ignificant featur�s to Tertiary erosion and denudation C)Cles . Two cycles can be clearly distinguslhed. While the Cumberland Plateau surfacP. origi11ated unde r humid tropical morphodyna�cs , the cumberl�d �esta and adjacent parts of the Highland Rim to a large extent are due to karstroorphological processes. Features of the Cumberland cuesta were changed only to 3 minor extt:!nt by Pleistocene , o••rbg to a negligible change in ba:;e lewl and the location of the CUmberland Plateau beyond the Pleistocene periglacial area.

Bogucki, D. J., 1970 , Debris slides and related flood damage associated with the September 1, 1951, cloudburst in the Mt . LeConte-Sugarland Mountain area, Great Smoky Mountain National Park [Ph.D. thesis ]: Knoxville, TN, University of Tennessee , 164 p. Des�ribes slide scar heads in detail . Tested effectiveness of aerial infrared imagery to detect the scars. nescribes scil characteristics .

Bogucki, D. J. , 1976, Debris slides in the Mt . LeConte area, Great Smoky Mountains National Park, U.S.A. : Geografiska Annaler, v. 58A, �· 179-191 . Discusses slides that took place September 1, 1951 . Describes slide tracks in detail . Also describes soils, vegetation, and sllde deposits.

Bollinger, G. A., 1973, Seismicity and crustal uplift in the southeastern United States: Auerican Jou�l of Science , v. 273-A, p. 396-408 . Suggests that strain development induced by crustal upl ifting but concentrated by old Appalachian structures may be the proximate cause of the recent seismicity in the southeaste:n United SLates. P�rtinent for neotectonics.

Bollinger, G. A. , 1973, Seismicity of the southeastern United States: Seismological Society of America Bulletin, v. 63 , p. 1785-1808 . Pertinent for neotectonics .

Bollinger, G. A. , and Sibol , M. s. , 1985, Seismicity, seismi c reflection studies, gravity, and geology of the central Virginia seismic zone : Part I. Seismicity: Geological Society of America Bulletin, v. 96, p. 49-57 . Pertinent for neotectonics. Seventy-five percent of the focal depths are 11 km or less .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bollinger, G. A. , and Wheeler, R. L., 1982, The Giles County, '!ir-;,inia, seismogenic zone- sei smological results and get.' "'gical interpretati:ms: U.S. Geological Survey Open-File Report, v. 82-585, 136 p. Describes and intPrprets a newly-recognized 40-!m-lnng seismo genic zone which is inferred to have been the locus of a damaging earthquake in 1897 . The zone seems most likely to have resulted from compressional reactivation of late Paleozoic compression and Mesozoic extension. The present-day motion on the inferred northeast-strikinj faul t or fault zone is such that ':he southeast side is I'!'OVing dowr. rel;ttive to t.'1e northwest side. Whether motion is reverse or normal is unknown , but the former appears more likely because the zone probably dips steeply NW and bec3use the region is probably under easterly-di rected compreasion at seismogenic depths.

Bollinge r, G. A. , and Wheeler, R. L., 1983, The Giles county, Virginia, seismic zone : Science , v. 219, p. 1063-106J. A short version of the authors' open-file report. Pertinent to neotecto:1ics.

Bonnett, R. B., 1975, Pleistocene and Holocene drainage changes northweat of the Nitro, west Virginia regio11: west Virginia Academy of Science Proceedings , v. 47, p. 205-211. Drainage in the Huntington-Nitro-Pt . P1eas< triangle or West Vi rginia is complex . �·idences of stream piracy, diversion, and abandonment are common and are related to the abandonment of the preglacial Teays River system and establishment of the Ohio-Kana·� system. The best examples of changes a.re afforded by Hurricane C�eek and its S�Veral Lributaries.

Bonnett , R. B. , 1977, Stream piracy: With example in southwestern west Virginia, in Adkins, H. G. , Ewing, S. , and Zimolzak , G. E. , eds., wrst Virginia and Appalachi3: Selected readings : Dubuque , I��. Kendall-Hunt Publishing Co., p. 37-48 . Piracy by an eastward flowing, westward cutting, trib<.�tary to the ea:ly Kanawha Riv&r beheaded Hurricane Creek and reversed it along with ita tributaries. This probably occurred very soon after the Kanawha itself was established, possibly due to piracy by the early middle Ohio River near Pt. Pleasant , We st Virginia. Thick alluvial valley fill played an important role in this diversion because it �Jld have generally smoothed out many topographic :ows, allowing newly developing streams responding to deglaciation �o have greater flexibility in establishing th�ir channels.

Bonnett, R. B. , Sanderson, D. D. , ane Noltimier, H. c., 1983, Teays Valley stratigraphy and magnetic dating of sediments in West Virginia [Abstract]: Geological Society of America Abstracts with Programs, v. 15, p. 529. Deposition in the Teays valley hke created by Pleistocene ice daDming probably occurred between 0.97 to 1.70 m.y. u .P. Diversion and abandonment of this segment �f the Teays River is thought to have involv� divide topping and piracy at both the west end of the valley by an early Ohio R:.-ter segment , and at t.!'le east end by a precursor stream to the modern lower Kanawha River.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bowman, I., 1911 , Forest physiography : New Yo rk , Wi ley, 750 p. ct.apters 28-32 deal with Appalachian physiography . Chapter 28 has a good sl.ll'liMry of the "Appalachian problem" up to that time .

Bowman, J. F. , II, and Lodding , w. , 1969, The Pensa·Jken Formation - a Pleistocene fluvial deposit in New Jersey, in Subitsky, S., ed ., Geology of selected areas in New Jersey and eastern P€:nnsylvania and guidebook of excursions: New Bnmswick , NJ, Rutgers unive1:si ty Press, p. 3-6 . Occurs along the southeastern margin of the Triassic Lowlands of �w Jersey and in scattered patches throu9hout the Coastal Plain. The main outcrop relt must have been the locus of a stream or stream system flowing southwest. The floral suite and lateritic-type weathering suggest that the Pensauken was deposited during a relatively warm interglacial period.

Brakenridge , G. R., 1983, Late Quaternary floodplain sedimentation along the POllllle de Terre River, southern Missouri . Part II: Notes on sedimentology and pedogenesis: Geologisches Jahtbuch , v. 71-A, p. 265-283. Describes a complex local history of flood pla�n sedimentation. Six alluvial formations have been mapped in the valley, and they form three topographically distinct fill terraces or terrace-compl"xes, one buried terrace , and the modern flood plain. Climatically induced changes in the rate of eolian influx of fine silt and clay, as well as local changes in precipitation and the nmoff/rainfall ratio, together were im(XJrtant controls over fine sediment composition and deposition rates.

8rakenridge , G. R. , 1904 , Alluvial stratigraphy and radiocarbon dating along the Duck River, Tennessee : Implications rega,rding flood-plain origin: Geological Society of America Bulletin, v. 95, p. 9-25. Four lithostratigraphic alluvial f•)rmations and eight chronostratigraphic subdivisions occur along the middle Duck River Valley. On the basis of nume rous excavat.o.ons and 14 radiocarbon dates , a history of flood-plain sedimentation can be traced. Results suggest the important:e of environmental controls at time scales of 100 to 10,000 yr. The stratigraphic information also indicates that after periods of stability and soil develorment and in respons- to altered hydrologic regimes , the Duck River forms new flood pla. t • latP.ral and vertical suspended-load accretion on channel ba.. s and in-channel bars. 1\t the sane time, the olde r flood-plain surface is covered by as much as several meters of the younge r alluvium and becomes a terrc:1ce . In contrast, lateral accretion of point-bar sands and gravels is not an important flood-plain forming process along t�is river.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Brakenridge , G. R. , 1985, Rate estimates for lateral erosion based on radiocarbon ages, Duck River, Tennessee : Geology, v. 13, p. 111-114 . Rates of bedrock erosion by ingrown meandering rivers can be inferred from the location of buried relict flood-plain and river-bank surfaces, associated paleosols, and radiocarbon dates. Two independent methods are used to evaluate the long-term rates of limestone bedrock erosion by the Duck River. Results for lateral migration are 0.6-1 .9 mvlOO yr and 0.5-1 .4 mvlOO yr . Findings show that lateral bedrock erosion by this river could have occurred coevally with flood-plain and terrace formation and that the resulting evolution of valley meander Lends carved into bedrock is similar in many respects to that of channel meanders cut into alluvium.

Braun, D. D., 1976, The relation of rock resistance to incised meander form in the Appalachian Valley and Ridge province [Ph.D. thesis]: Baltimore, Johns Hopkins university, 248 p. Form and dimensions of bedrock meande rs are related to type and character of the bearock .

Braun, D. D., 1983, Lithologic control of bedrock meander dimensions in the Appalachian Valley and Ridge province: Earth Surface Processes and Landfc�. v. 8, p. 223-237 . Marked differences in bedrock meande r dimensions are related to differences in relative erodibility of the bedrock . Meanders cut in thick-bedded to �ssive lithologies, typically carbonates, are distinctly smaller ove•all than meande rs cut into shaly lithologies.

b.Letz, J. H., 1942, Vadose and phreatic features of limestone caverns : Journal of Geology, v. 50, p. 675-811 . Genetic r.lassification of patterns and features is attempted with the purpose of establishing criteria for both phreatic and vadose origin . In many caves, an epoch of clay filling occurred after the phreatir. solution ceased and befor< a lowering wat�r table allowed the formation of free-surface streams. l�st caves are out of adjustment with the topography of their region and therefore are older than the present cycle of erosion.

Bretz, J. H. , 1953, Genetic relations of caves to pene�lains and big springs in the Ozarks: American Journal of Science , v. 251 , p. 1-24. During old age , cave-making ceased as hydrostatic head disappeared wi th reduction of the uplands . To a large extent the existing caves then became filled with residual red clay filtered down from the peneplain soil. Remnants of this clay fill are considered as valid a record of peneplanation as are the flattish uplands bevelling structure. Later upl ift caused deep dissection of the peneplained dome. This lowered the water table and brought most of the caves into the vadose zone .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bretz , J. H. , 1962, Dynamic eTJilibrium and the Ozark land fonms: American Journal of Science , v. 260, p. 427-438 . Significant ge�rphic features and their relationships in the Ozarks record events and sequences that are illp)ssible by the noncyclic theory of dynamic equilibrium. Only the Davisian concept of cycles of erosion separated by recurrent uplift of the Ozark dome will account for the region's geomorphic history.

Bretz , J. H. , 1965, Geomorphic history of the Ozarks of Missouri : Missouri Division of Geological survey and Water Resources, Second Series , v. 41, 147 p. The succession of events is seen as foliows : 1) A probable early peneplanation suggested by summit altitudes of Boston Mountains in Arkansas; 2) A uplift that rejuvenated the radial pattern of rivers flowing off the ozark dome launched a new erosion cycle wh ich destroyed the Boston Mountains peneplain and produced the lower Springfield peneplain; 3) A later and larger uplift initiated the ozark cycle of erosion which destroyed much of the Springfield surface . The Ozark peneplain was in turn deeply dissected by a later uplift. Remnants are the nearly baseleveled upland plains , only slighltly warped by domal uplift.

Bridge , J., 1950, �uxite deposit3 of the southeastern United States, in Snyde r, F. G. , ed. , Sympositllll on mineral resources of the southeastern United States, 1949 Proceedings : Knoxville, University of Tenne ssee Press, p. 170-201. Seeks to supplement Adams (1927 ) who considered bauxite to originate as a result of ordinary processes of weathering, transportation, deposition , and subsequent alteration. Notes that in any given district the re is a preferred altitude at which the deposits are found. Deposits in the V&R appear to be filled sink deposits. Strong suggestion that they are only the roots of deposits that formerly were much larger. Lignite commonly occurs in clays enclosing the b' �ite - as old as early Te rtiary. Suggests chief source'· · erial was crystallines of Piedmont and Blue Ridge. Streams f: from these areas onto the Ha rrisburg surface or onto a coast�- plain of the same age .

Briggs , R. P. , 1974, Map of overdip slopes that can affect lands' '.ding in Allegheny County, Pennsylvania: u.s. Geological survey Misct.llaneous Field Studies Map, v. 543, 1 p. Map showing areas with overdip slopes in which rock layers dip 40 to 100 ft/mile and those in which rock layers dip more than 100 ftjmile . Indicate, to some degree , susceptibility to landsliding.

Briggs, R. P. , Pomeroy, J. S. , and Davies, W. E. , 1975, Landsliding in Allegheny County, Pennsylvania: u.s. Geological Survey Circular, v. 728, 18 p. To accompany "llap of susceptibilty to landsliding, Allegheny County , Pennsylvania:" u.s. Geological Survey MiFcellaneocs Field Studies Map MF-685B . semi-popular.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Brown, B. W. , 1967, A Pliocene Tennessee River hypothesis for Mississippi : Southeastern Geology, v. 8, p. 81-84 . Author hypothesizes that the discontinuous gravel-defended ridges which extend southwestward from Scott County, Misr.issippi , through Brookhaven are relict deposits from a Pliocene river course that may have been a southwestward extension of the �lacbian-Tennessee River trend . Anomalous southeastward drainages in southern Mississippi are explained by this h�pothesis.

Brown, D. A. , 1971 , A Kentucky solution cuesta revisited; an alternative explanation: Association of Americ� Geographers Proceedings, v. 3, p. 38- 40. Solutional processes have been advanced as the meC"hanism responsible for the relief of the Dripping Spring escarpment and for the basin karst topography at its base. Field examination of soils, recently published soils analyses, and trend surface analysis of the topography suggest normal fluvial erosion as an alternative explanation .

Brown, E. H. , 1961 , Britain and Appalachia - A study in the correlation and dating of planation surfaces: Institute of British Geographers Publication , v. 29, p. 91-100. Author attempts to correlate the Harrisburg, Schooley, and Upland peneplains in the Appalachians with peneplains in Great Britain. Fig. 2 shows this correlation graphically.

Brown, L. , Tera, F. , Valette-Silver, N. , Pavich, M. J., Klein, J. , and Middleton, R. , 1986, Application of lOBe to the study of erosion and sediment transport, ir. Proceedings of the Fourth Federal Interagency Sedimentation Conference, March 24-27 , 1986, Las Vegas, Nevada: Interagen. Advis. Comm. W��. Data, p. 4-10 to 4-19 . By measuring the lOBe concentration in the sediment carried by a stream from a basin, one can compare (provided sediment transport oata are available ) the rate at which atoms leave the basin with the rate at which they are deposited in it. OWing to the large inventory known to exist in soils and to decay th�re, this ratio must be less than unity for steady-state lOBe deposition and erosion. Despite the problems of selecting samples of sediment that match the average sediment transported by the stream from tha basin, results give fairly consistent picture. Of particular note is the clear indication of enhanced sediment I!DVement in the Piedmont but not in the Coastal. Plain. 'lhis accelerated erosion may reflect the introduction cf agriculture on a large scale , but it may also reflect Quaternary climatic change or accelerated tectonic uplift.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Brown, L. D. , 1978, Recent vertical crustal movement along the east coast of the united States: Tectonophysics, v. 44, p. 205-231 . Pertinent for neotectonics . Results from leveling seriously conflict with those obtained from secular trends in sea level . At least one of the method.; must be seriously affected by some systematic non-tectonic influence. Despite these inconsistencies, the apparent crustal movements correlate with regional elements of geologic structure , particularly the Conr�cticut Va lley graben, the Chesapeake-Delaware embayment, the Cape Fear arch, and the Cape Canaveral prominence .

Brown, L. D., and OlivP.r, J. E. , 1976, Vertical crustal movements from leveling data and their relation to geologic structure in the Eastern United States: Reviews of Geophysics and Space Physics, v. 14, p. 13-35. Rates of relative vertical motion are commonly too large to be attributed to leveling errors and therefore must reflect true earth movements. With some exceptions, modern movements appear to be relatP.d to earlier Phanerozoic trends, but the rates of modern movements are much larger than average rates over the past 130 m.y. Thus movements are either episodic or oscillatory about a long-term trend. The Appalachian Highlands are rising relative to the Atlantic Coast at rates of up to 6 romvyr . Elongated zones of relative uplift and subsidence paralleling eithe r the Appalachian drainage divide or the trend of Appalachian structure are suggested. The maxima correlate strongly with topographic highs .

Brown, L. D., Reilinger, R. E. , ar.d Citron, G. P. , 1980, Recent vertical crustal movements in the u.s.: Evidence from precise leveling, in Marner, Nils Axel, ed., Earth rheology, isostasy, and eustasy, proce�dings of a symposium, Stockholem, 1917 : New York , Wiley, p. 389-405. Authors discus� a level route across the Appalachians in Nortll Carolina and Tennessee . The region in the vicinity of the Brevard fault zone W3S characterized by a distinct pattern of up1.ift relative to other pcntions of the lim!. Of primary interest is the fact that the maximum apparent net elevation change in the upar ched zone occurs at the drainage divide, only about 10 km west of the Brevard zone . This correlation seems to be too close for mere coincidence, and thus a causal relationship between the apparent uplift and the geologic and/or geomor9hic features is suspected. There is a strikin�r correlation between the apparent elevation changes and topography along the route . such a correlation can be suggestive of elevation-correlated levelling er�ors. on the other hand, it is not unreasonable to suspect that areas which are unde rgoing comtemporary uplift are the same areas exhibiting the greatest topographic relief.

Brucker, R. w. , 1966, Truncated cave passages and terminal breakdown in the Central Kentucky Ka rst: NSS Bulletin, v. 28, p. 171-178. Author discusses cave passages in MalllllOth Cave National Park that have been truncated by breakdown. Segments of formerly continuous passages have similar size, shape , elevation, alignment, and cross section. Wall scallops indicate a former c�n direction of water flow. unde rstanding of the process of truncation and recognition of its results leads to reconstructions of past cave patterns.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Brucker, R. w. , He ss, J. w. , ann White, w. B. , 1972 , Role of vertical shafts in the movement of ground water in carbonate aquifers: Ground water, v. 10, p. 5-13. Vertical shafto form the headwater termini of complex drainage networks that aggregate the waters into master drains which carry the water to big springs . The drains evolve through time as base level is lowered but retain a dendritic pattern. Shafts are very short lived and occur only near the edge of the clastic caprock in th_ -tudy area. Shafts are formed by free-flowing sheets or films of vadose water streaming down the walls in supercritical flow. There is a measurable uptake of calcium carbonate as the water traverses the shaft Vcllls. The shafts act as aeration chambers, and there is much loss of carbon dioxide from the ground water during movement through this segment of the underground route.

Bruner, D. H., 1972, The influence of cap rock on the development of slopes : A quantitative analysis of slopes developed on two sequences of flat-lying carbonate rocks in the presence of and in the absence of resistant sandstone cap rocks (southwestern Kentucky ) [M.S. thesis]: Terre Haute , IN, Indiana State University, 75 p. Author finds that carbonate slopes developed in the presence of caprock are significantly steeper than those developed in the absence of caprock, that slopes developed in the Paint Creek limestone section are steeper than those developed in the Renault limestone sequence, and that there are obvious contrasts among the forms of the histograms depicting the mean and maximum slopes developed in the two carbonate sections (both in the presence and absence of caprock ). Thinks main effect of caprock is to prevent as much water from reaching the underlying carbonates.

Brunnschweiler, D. , 1962, The periglacial realm in North America during the Wisconsin Glaciation: Biuletyn Perglacjalny, v. 24, p. 233-244 . Briefly mentions periglacial features in the Piedmont and Coastal Plain provinces.

Brush , L. M., Jr., 1961, Drainage basins , channels, and flow characteristir.s of selected streams in central Pennsylvania: u.s. Geological Survey Professional Paper, v. 282-F, p. 145-181 . Hydraulic, basin, and geological characteristics of 16 selected streams were measured for the p�..rpose of studying the relationship among these general characters and their processes of development . Measured bankful width and depth, channel slope, bed material size and shape , length vf stream from drainage divide , and size of drainage area. Excellent correlations were found to exist between drainage area and the 2.3-year flood. As there was also an excellent relationship between length of stream and drainage area, it is possible to predict discharge for the 2.�-year flood at any point along the length of the stream. Particle size decreases downstream in many streams but remains constant or increases in others. A stream channel underlain by sandstone tends to have a steeper slope and larger bed material than channels undP.rlain by shale or limestone .

1�

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Bryan , K. , 1940, Gully gravure - a method of slope retreat : Journal of Geomorphology, v. 3, p. 89-107 . In discussing his theory of gully gravure , Bryan include� one example from the Blue Ridge of North Carolina .

Bryan , K. , 1940, Soils and periglacial phenomena in the Carolinas : Science , v. 91 , p. 523-524. Mainly reiterates Eargle 's (1940 ) findings concerning colluvium in �o Piedmont .

Bryan, K., Cleaves , A. B. , and Smith, H. T. U. , 1933, The present status of the Appalachian problem: Zeitschrift fur Geomorphologie, v. 7, p. 312-320. Summarizes previous work on and major questions concerning erosion cycles and drainage evolution in the Appalachians .

Buol, s. W. , 1973, Soils of the southern states and Puerto Rico: Southern Cooperative Series Bulletin, v. 174, 105 p. Describes soils of Virginia, Kentucky, and all states south . Publ ished by Soil Conservation Service.

Burford, A. E., 1966, Drainage patterns of the Appalachian Plateau province : West Virginia Academy of Science Proceedings, 1965, v. 37 , p. 160-166. Drainage pattern of Plateau is grossly dendritic, but various other types of patterns occur and commonly either dominate or markedly modify the general pattern. Patterns , which include angulate , rectangular, trellis, radial, and annular, reflect both fairly obvious and extremely subtle structure control by joint sets and system� , by small and large flexures, and by broad, inconspicuous domes.

Burtnett, J. W. , 1966 , The role of systematic lateral stream migration in the development of drainage basins and asymmetrical valleys [M.S. thesis): University Park, Pennsylvania State university, 65 p. Schumm (1956) reported that entrance angles of streams changed with changes in the gradient ratios of the converging streams . He thought that this change in angle was partially accomplished by the migration of the tributary channel toward the main chcudlel . Thesis seeks to verify this observation, and also to determine the role of systematic stream migration in the creation of asymmetrical valleys. Concludes that role of lateral stream migration is not significant. Author suggests that a�rently, after a stream incises itself, its entrance angle will not change with changes in the gradient ratio.

Butts , C., and Moore, E. S., 1936, Geology and mineral resources of the BellefontP. quadrangle: u.s. Geological Survey Bulletin. v. 855, 111 p. Describes topography and drainage of area, includ�ng erosion cycles .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Cady , J. G. , 1951 , Rock weathering and soil formation in the North Carolina Piedmont region: Soil Science Society of America Proceedings , v. 15, p. 337-342. A soil derived from meta-gabbro and one de rived from diorite , a few miles apart, were studied by means of thin sections , x- ray spectrometry, and other mineralogical methods . The soil from diorite was unde rlain by 20 ft of saprolite while the other profile graded into solid rock at about 4 ft. First-weathering products of the diorite were gibbsite, chlorite, and allophane . In later stages these minerals had disappeared and coarsely crystalline kaolinite, primary and secondary quartz, and iron oxides had entirely replaced the entire rock . Feldspar of the meta-gabbro weathered to halloysite almost completely before the ferro-magnesian mir-.erals start:.ed to alter noticeably. In the A and B horizons an ac�AIL.ation of �Jartz indicated a large loss of weathering product;;, yet fresh hornblende and feldspar were abundant in all horizons . Continual addition of this mineral to all horizons by sloughing from boulders and pebbles is suggested as their source.

Cain, s. A. , 1944, Pollen analysis of some buried soils, Spartanburg County, South Carolina: Torrey Botanical Club Bulletin, v. 71 , p. 11-22. Pollen analyses of profiles of four of these buried soils indicate that their age is sufficient to relate them to cooler climates than today, probably Pleistocene . Pollen grains of Picea and Abies are more abundant in the lower half of the deposits, a fact that provides an indication that the sediments accumulated unde r a warming climate.

Calvert, C. S., Buol , S. W. , and weed, S. B. , 1980 , Mineralogical characteristics and transformations of a vertical rock-saprolite-soil sequence in the North carolina Piedmont : I. Profile morphology, chei!Ucal composition, and mineralogy: Soil Science Society of America Journal , v. 44, p. 1096-1103. Soil was a Typic Hapludult formed on granite gneiss . Profile was sampled in 19 horizons, from surface to slightly altered rock . The most rapid chemical changes occurred in the deepest saprolite horizons .

calvert, C. S., Buol , S. W. , and Weed, S. B. , 1980 , Mineralogical characteristics and transformations of a vertical rock-saprolite-soil sequence in the North carolina Piedmont : II. Feldspar alteration products - their transformations through the profile. Soil Science Society of America Journal, v. 44, p. 1104-1112. The initial weathering of feldspar at the rock-saprolite contact is very rapid and results in a variety of minerals, each formed within a specific microenvi ronment. Electron microscopy and other techniques confirmed the direct formation of halloysite, amorphous aluminosilicates and gibbsite. These same techniques also suggested the resilication of tt� latter two minerals into tubular and tabular halloysite, respectively. Somewhat higher in th� profile the halloysite recrystallizes into :

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Cameron, c. C. , 1970, Peat resources of the unglaciated uplands along the Allegheny structural front in we st Virginia, Maryland, and Pennsylvania: u.s. Geological Survey Professional Paper, v. 700D, p. Dl53-Dl61 . Largest deposits are in Canaan valley, West Virginia. Peat deposits of the filled-basin type , restricted to terraces, divides , or interfluves in large structurally controlled valleys , are potential resources. Describes sedimentary characteristics of peat in different types of topographic settings .

Came ron , E. N. , 1951 , Feldspar deposits of the Bryson City district, North Carolina: North Carolina Division of Mineral Resources Bulletin, v. 62, 100 p. Briefly describes topography and physiography. Also notes that exposures in mine and prospect openings in nearby areas indicate that [colluvhun] has moved, in considerable part, by sliding on well-defined surfaces.

Campbell, M. R. , 1894, Tertiary changes in the drainage of southwestern Virginia: American Journal of Science , v. 48, p. 21-29. Guest River, from the Norton divide to Coeburn, exhibits unmi stakable evidence oi a reversal of its course. All the tributaries in this interval turn westward to join �� e river which flows due east. The present position of these tributaries is found to bear no particular relation to the geologic structure. The acute angle made by Guest River itself at Norton is equally remark�ble . Suggests local isostatic uplift, after the Tertiary period of base leveling, caused the reversal of this reach of the river.

Campbell, M. R., 1896, Drainage modifications and their interpretations : Journal of Geology, v. 4, p. 567-581 , 657-678. Discusses recent crustal movements influencing Tennessee River at Muscle Shoals. Also discusses changes in Kanawha River, Big Sandy and Clinch rivers, river basins of Kentucky, Chattahoochee River, and others

Campbell, M. R., 1897, Erosion at base leve�: Geological Society of Americ� Bulletin, v. 8, p. 221-226. Using examples of local bas�levelled surfaces in West Virginia, argues that the level floors of such surfaces have too low a grade to mechanically transport rock debris, and that much of the latter must be removed by solution . Therefore, concludes that intense chemical action must be an important agent of land sculpture on a surface near or at base level.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Campbell , M. R. , 1897, The origin of some mountain scarps [Abstract ]: American Geologist, v. 17 , p. 408 . Outlines hypotr�sis for origin of Blue Ridge escarpment . It is the result of a slow monoclinal uplift modified by erosion. Notes that area to the south�ast , unaffected by the uplift, should have remained at base level . If the movement was relatively rapid, the lower peneplain would encroach but slightly upon the uplift. If the movement was slow, the peneplain would encroach to a muc)"' greater extent not only along the streams, but also in the inter-stream areas. The result of this encroachment would be to accentuate the slope produced by the uplift. If the movement is extre!IIP.ly slow, the slope becomes a scarp, which the author believes is what happened .

C�bell, M. R. , 1903, Geographical developuent of northern Pennsylvania and southern New York : Geological Society of America Bulletin, v. 14, p. 277- 296 . Mainly a comparison and correlation of erosion surfaces. Author recognizes remains of 2 peneplains : a lower late Tertiary SU Y�ace , carved only on softer rocks, and an early Teriary surface , the Harrisburg peneplain. Correlates latter surface with a peneplain in SW Pennsylvania and adjacent Ohio. Map shows warped surface of the Harrisburg penplain.

Campbell, M. R. , 1929, Geomorphic value of river gravel : Geological Society of America Bulletin, v. 40, p. 515-532. Mainly a general discussion, but applies his theory to high gravels of the Susquehanna. Upper gravel called Bryn Mawr , lower one , Brandywine. Latter gradually .·ises in elevation upstream, while Bryn Mawr appears to have ur�e :gone deformation before deposition of the Br<'ndywine by an uplift whose axis crossed the river near Safe Harbor . Maximum uplift about 280 ft.

campbell, M. R. , 1929, Late geologic deformation of the Appalachian Piedmont as determined by river gravels: National Academy of Science Proceedings , v. 15, p. 156-161. Discusses possibility of discovering slight flexures in the Piedmont by careful tracing of high-level gravels which are known to occur near the mouths of rivers crossing this belt. Higher and older gravel bed along Susquehanna is generally recognized as having been deposited in late �ertiary time, but long antedating the Pleistocene . This bed called Bcyn Mawr , and below it is a lower bed , the Brandywine . The Bryn Mawr gravel, which at the mouth of the river is 100 feet al� e the Brandywine gravel, rises until at safe Harbor it is 270 ft a..'mre the same bed . Upstream from there it gradually descends until at Middletown it is only 70 ft above it. Interpretation is that the Bryn Mawr has been defo� into an anticline whose axis crosses the river at Safe Harbor .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 campbell , M. R., 1931, Alluvial fan of Potomac River: Geological Society of America Bulletin, v. 42, p. 825-852 . Concludes that the surface materials on the Coastal Plain werP deposited on a plain sloping very gently south or �outheast toward the sea, the margin of which was the Surry beach in Virginia , whose present altitude is 90-100 ft. The Brandywine gravel is a true alluvial fan composed of sand and gravel brought down by the Potomac River.

Campbell, M. R. , 1933, Chambersburg (Harrisburg) peneplain \n the Piedmont of Maryland and Pennsylvania: Geological Society of America Bulletin, v. 44, p. 553-573. Traces Harrisburg peneplain into Piedmont by using benn gravel . Concludes that berms on Potomac are the same as those on the Susquehanna . Figure 3 shows the deformation of the Bryn Mawr benn and of the Chambersburg (Harrisburg) peneplain. Estimates the Chambersburg peneplain is 300 ft above the Bryn Mawr gravel. Based on amount of rock material removed and erosion rates, estimates an age of early Miocene for the Chambersburg and early Pl iocene for the Bryn Mawr berm.

Campbell, M. R. , and Ba�r0m, F. , 1933, Origin and structure of the Pensauken gravel: American Journal of Science , v. 26, p. 300-318. Authors consider sou&.ce of the material in the deposit, the means by which it was transported to this locality, the conditions under which it was deposited, and the possibility of deformation subsequent to its depo&ition.

carey, J. B., Cunningham, R. L., and Williams , E. G. , 1976, Loess identification in soils of southeastern Pennsylvania: Soil Science Society of America Journal, v. 40, p. 745-750 . Tha physical properties, sorting coefficients , and homogeneity indicate that a silty mantle generally 1 m thick in southeastern Pennsylvania is loess. The lllililtle's geographic location , gradation in thickness , and ve ry fine sand content indicate that the Coastal Plain and the adjacent rivers are probable source areas for the loess.

Carlston , c. w. , 1946, Appalachian drainage and the highland border sediments of the Newark seriPs: Geological Society of America Bulletin, v. 57, p. 997 .. 1031. No extraordinary correlation was found between the highland border sediments of the Newark series and the present drainage of the central and northern Appalachians. There is, further, no evidence of major stream deposition of the highland border fanglomerate&, nor evidence that any present-day stream enters the Newark basin through Triassic-filled remnants of Triassic valleys . Thus , the highland border sediments of the Newark basin fail to provide evidence for Triassic or pre-Triassic origin of the present drainage .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Carlston , c. w. , 1962, Character and history of the uppe r Ohio River valley: u.s. Geological Survey BullPtin, v. 1141-I , p. Il-IlO. Dismemberment of the preglacial Teays Valley system and develop ment of the present Ohio River valley began in late Tertiary or early Pleistocene . By Illinoian time the present Ohio River was largely established in its present course, except for its headwaters above mile 114, which still flowed northward. The Illinoian glacial advance into northwestern Pennsylvania caused diversion of this portion of the Ohio River into its present course . 'Ihe bedrock valley was deepened and broadened during the Sangamon interglacial stage, and was filled with fluvioglacial deposits during Wisconsinan ice advances .

Carlston , c. w. , 1969, Longitudinal slope characteristic� of rivers of the mid continent and the Atlantic east Gulf slopes: Interna��onal Association of Scientific Hydrology Bulletin, v. 14, p. 21-31 . Author prepared a large number of longitudinal profiles of graded alluvial-bed rivers. The east�rn Midcontinent river.s, such as the Ohio River above Louisville and the Tennessee River above Muscle Shoals, are low in gradient, but show noticeable bedrcck-produced irregularities. Their profiles are nonsegmented, concave-upward, and are regarded as ungraded . Rivers of the Atlanti� Slope and East Gulf Slope have straight constant slope graded segments in the Coastal Plain but steep and highly complex profiles above the Fall Line . This suggests repeated epeirogenic movements of the Atlantic seaboard, some involving the entire continental block , and others only parts of it.

carroll, D. , 1959, Sedimentary sLudies in the Middle River jrainage basin of the Shenandoah valley of Virginia: u.s. Geological Survey Professional Paper, v. 314-F, p. 125-154. Author examined di&·�ribution and lithology of principal rocks of the area, the amount and mineralogic c�sition of their insoluble residues, the kinds ?f soils formed from them, their grain size and mineralogic composition. Also, the alluvial , terrace , and high flood-plain soils, their grain size and mineralogic composition; and the mineralogic composition of sands in the river and stream bed. Concludes (for exa��ple) that sandstones of Devonian age were more actively eroded by thP Middle River in the past than n0\'1 .

Carter, B. J., and Ciolkosz, E. J. , 1980, SOil temperature regimes of the central Appalachians : Soil Scien�e Society of America Journal, v. 44, p. 1052-1058 . The derived temperature prediction equation indicates that the mesic-frigid soil temperature boundary rises rapidly in elevation from north to south and that there are areas of Pennsylvania, Maryland, west Virginia, and Virginia thathave fri�id soil temperature regimes. The mean annual air temperature averages 1.2 degrees C below the mean annual soil temperature.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 carter, B. J., and Ciolkosz, E. J., 1986, Sorting and thickness of waste mantle material on a sandstone spur in central Pennsylvania: Catena , v. 13 , p. 241-256 . Authors used soil pits and haltmer seismograph to study colluvium on a sandstone ridge . Also measured particle size, sorting, and fabric of the collUV\DII. Depth to bedrock ranged from 3.0 to 6. 3 meters. The upper 1.4 mat all sites was modified by periglacial denudation evidenced by lobate solifluction terraces and subsurface and surface rock sorting. Authors think findings best explained �· deep weathering over thousands of years followed by severe periglacial f(ost action and denudation during the last Wisconsinan glacial advance .

Chambe rlin, T. c. , and Leverett, F. , 1894 , Further studies of tha drainage features of the uppe r Ohio basin: American Journal of Science , v. 47, p. 247-283. Authors attempt to infer preglacial drainage in the upper Ohio basin, and to determine the manner in which changes took place as a consequence of glaciation.

Chapnan, J. , 19/o, The Archa1c period in the lower Little Tennessee River valley: 'r'he radiocarbon dates: Tennessee Anthropologist, v. 1, p. 1-12 . Author discusses 19 radiocarbon dates on charcoal in an archeological context.

Chapnan, J., Delcourt, P. A. , Cridlebaugh , P. A., Shea , A. B. , and Delcovrt, H. R. , 1982, Man-land interaction: 10,000 years of American Indian impact on native ecosystems in the lower Little Tennessee River valley, eastern Tennessee: Southeastern Archeology, v. 1, p. 115-121. Stratified archaeological deposits from the Little Tennessee River watershed have yielded a 10 , 000-yr record of vegetational change reflecting both geomorphic events and the utilization of �l�nt resources by Amer::.can Indians . Changes in composii:.1on of charred wood , fruit, and seed assemblages indicate the progressive impact of man upon the native vegetation.

Charron, M. A., 1977 , An examination of some drainage basin relationships in southwestern Pennsylvania [M.A. thesis): Pittsburg, university of Pittsburg, 130 p. A less-·than rigorous study relating some geologic, pedologic, and morplaaaetric parameters to stream flow. However, flow was measured only during the fall of one year , by measuring surface velocity. Also, relation of parameters to stream flow was not done systematically.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Chorley, R Climate and morphometry: Journal of Geology, v. 65, p. 628-6j

An • <>J.S of tl.·, morphometry of three areas (in Ptmnsylvania, AlabaJ!o.a, and Exmoor, England ) with similar gross lithology, st�uctural effect, and stage of dissection was carried out . A climate/Vegetation index was obtained for each region, employing the mean annual rainfall , the mean monthly maximwn precipitation in 24 hours, and Thornthwaite's precipitation effectiveness index. It was found that the index bears a remarkably con�istent relationship to the 'Ale&• logarithms of stream lengths , basin areas, and drainage dtmsiti es.

Chorley, R. J., arad Morgan, M. A. , 1962, Comparison of oorphometric features, Unaka Mountains, 'l:ennessee ancl. North Carolina , and Dart.Jooor, England : Geological S?ciety of America Bulletin, v. 73, p. 17-34. Measured basin and stream oorphometric parameters in unaka Mountains and in DartiOOor. Concluded that the striking contrast in drainage densities between the two regions , on which most of t�e remaining morphometric diffe.�nces hinge , is explained mainly on the basis of the consistently �i. ffering rainfall intensities which the two region� experience .

H. � Christopher, R. A. , Prowell, D. C., Reinhardt , J. , and Markewich, •• 1980, Paleocene pollen trom warm Springs, Georgia - thei r stratigraphic and structural signiUcance : Palynology, v. 4, p. 105-124 . TWenty pollen species recovered from auger samples of an isolated pod of sediment indicate a late Paleocene age for the deposit. The sediments have beer. protected from arosion by faultir.y along the southern margin of the basin containing them. The structural relationships and the Paleocene age for the deposit provide evidence of Cenozoic tectonic 3Ctivity. Regional stratigraphic and sedimentologic evidence suggests thAt �� e deposit was probably a northward extension of the bauxite: dist.ric:ts of Ande rsonvi lle, \..e orgia, and Eufaula, Alabama.

Ciciarel.l.i, J. A. , 1971, GeCIIIOrphic evolution of anticlinal valleys in central Pennsylvania [Ph.D. thesis) : University Park, PA , Pennsylvania State university, 210 p. Author exemdnes anticlines that are in various stages of breaching and from this infers a gene ral sequence of breaching.

Ciciarelli, J. A. , 1984 , Structural control on breaching of an Appalachian anticline in central Pennsylvania: Northeastern C� ology, v. 6, p. 102-104 . Addressee question of what determines the location of the initial breaching point on a particular anticline . Studied Tuscarora Mountain Anticlin& , PA , uhich is in the early stages of breaching, and four.d it to be b!';.c.�ched at its structural "nigh ?Oint. A co1.1nt of frac·r.u··es visible on aerial photos shows a greater densily in the vicinit.� of thr� st.ructt!ral high, suggesting the reason that the structural high point :.s where initial breaching occurs.

Ciolk..:.:z, E. J. , 1978, Th� AgT.es flood: Permsyl··-.ni� �tate Uni·:ersity Agronomy Series, v. 52, �- 39-�0 .

Provides isopleth map for the total ·, " infall in Penn:--ylvania.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ciolkosz , E. J. , 1978 , Periglacial features of Pennsylvania: Pennsylvania State university Agronomy Series, v. 52 , p. 35-38 . Author briefly summarizes periglacial features, presumably relicts of the Pleistocene , in Pennsylvania. Map showing boulde r fields , grezes litees, ice-wedge casts, patterned ground, involutions .

Ciolkosz , E. J. , 1978, Soils of tne central Susquehanna valley: Pennsylvania State University Ag ronomy Series, v. 52 , p. 28-34. Briefly describes soils and soil-landscape relations . Fig. 4.1 sh��s soil-landscape relations.

Ciolkosz, E. J. , Clark, G. M. , Hack, J. T. , Sigafoos, R. s., �d Williams , G. P. , 1971, Slope stability and denudational processes : central Appalachians (Prepared for field trip 10 of the Geological Sociely of America , Washington Meeting, October, 1971 ): Wa shington, DC, Geological Society of Wa shington, 31 p. Mainly a road log, with only very brief descriptions , to various geomorphic features in the central Appalachians .

c. , Ciolkosz , E. J. , Cronce , R. Cunningham, R. � .• and Peterson , G. w. , 1986 , Geology and soils of Nattany Valley : Pennsylvania state University Agronomy Series, v. 88, 59 p. Geologic and geomorphic evolution, soils, and paleoclimate of the second-largest valley in the valley and Ridge province .

Ciolkosz, E. J. , Cronce , R. c. , and Sevon , w. D. , 1986, Periglacial features in Pennsylvania : Pennsylvania State university Agronomy Series, v. 92 , 15 p. Authors provide a table and maps showing locations of boulder fields, grezes litees , ice-wedge casts, pingos, patterned ground , solifluction lobes, and involutions , presumably relicts of Pleistocene times. There is also a brief discussion of colluvium and loess.

Ciolkosz, E. J. , Gardner, T. 'fl. and Dobos , R. R. , 1988 , Paleosols in Pennsylvania: Pennsylvani State Universtty Agronomy Series, v. 100, 9 p. After a brief discussion of the nature of �leosols, authors present a table and map that show locations of bu ried soils (and type of parent material ) that have been reported in Pennsylvania.

Ciolkosz, E. J. , Latshaw, G. J., Cunningham, R. L. , and Sevon, w. D. , 1971 , Parent material , topography , and time as soil-forming factors in eastcentral Pennsylvania: Pennsylvania state University Agror.omy Series, v. 21, 27 p. Authors discuss the effect of geology, geomorphology, and tirre on soil formation in the Triassic Lowland , the Readii.-J Prong , the Valley and Ridge , and the Glacidted Low Plateaus . They cor.�entrate on ten s0ils.

Ciolkosz , E. J. , Petersen, G. w. , and Cunningham, R. L., 1979 , Landslid�-prone soils of southwestern Pennsylvania: soil Science , v. 128, p. 348-352. Upshur, Vandergrift, Guernsey, and Library soils have high clay contents, high coefficients of linear exte�sibil ity , and slickensides, and are landslide prone . Other soils having high contents of clays other than expandable types are not subj ect to landslid�o;.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ciolkosz , E. J. , PetPrsen, G. w. , Cunningham, R. L. , and Matelski , R. P. , 1979, Soils developed trom colluvium in the Ridge and Valley area of Pennsylvania: Soil Scie11ce , v. 128, p. 153-162 . Colluvium unde rlies 27 % of area of unglaciated Valley and Ridge in Pennsylvani.a. Occurs on lower one-half to three-fourths of side slopes of major and secondary ridges . Simple side slope deposits extend about 1 km from ridge crests, and fan deposits about 0.5 to 1 k.n beyond the former. soils similar on both f-vpes of deposits . The presence of argillic horizons, fragipans , s1gnificant illite weathering, and appreciable leaching indicates that these soils are moderately well developed, implying that the landscapes on which they are formed probably date back to Wisconsinan glacial time .

Citron , G. P., and Brown, L. D. , 1979, Recent vertical crustal movements from precise leveling surveys in the Blue Ridge and Piedmont provinces, North caroiina and Georgia: Tectonophysics, v. 52, p. 223-238. Examination of two lines of repeated leveling in North carolina and Georgia reveals apparent uplift at L� e Blue Ridge-Piedmont physiographic boundary (Atlantic-Gulf drainage divide ) relative to land east and west. In NC a very pronounced correlation between topography and movement suggests possible systematic leveling error, but the observed movements appear to be larger than those normally attibutable to leveling error. Anomalously high stream-gradients ove r both resistant and nonresistant lithologies are common at and near the divide, and may be associated with the relative uplift inferred from releveling. The evidence thus suggests that stream morphology may be responding to contemporary deformation as implied by the observed elevation changes.

Clark, G. M. , 1967, Structural geomorphology of a portion of the Wills Mountain anticlinorium, Mineral and Grant counties, west Vi rginia [Ph.D. thesis): university Park, PA , Pennsylvania State university, 201 p. Author attempts to explain reason that many streams occupy ga�s through ridges underlain by relativ�ly resistant rock when alternate courses over less resistant strata were apparently available. Examines several hypotheses. Notes that along one anticlinorium, faulting or tight monclinal flexuring affecting tl1e entire thickness of the TUscarora sandstone exists at or near the crest in 4 of the 5 water gaps in which this rock is expos �. In 3 of these gaps , the TUscarora is highly fractured. Compara.Jle structural weaknesses are absent : n the areas between these gaps . The hypothesis of local supe rposition from an ove rlying weak roc': unit, modified to include the inferred role played by structural weakness, explains the observed relationships .

Clark, G. M., 1968 , sorted patterned ground : New Appalachiar localities south of the glacial b>rder: Science , v. 161, p. 355-356. Sorted stripes, nets, and polygons display patterns and stone orientations visibly similar to those of ground patterned unde r current cold climates. Larger forms appear inactive or fossil and may provide data on the paleoclimate and slope stability.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Clark, G. M. , 1969, Preliminary distribution, characteristics, and origin of some Appalachian sorted patterned ground localities south of the glacial border [Abstract ): Geological Society of America Abstracts with Programs, v. 1, p. 34 . Author supplements observations in his 1968 Science article on this subject. Patterned ground occurs above 450 m elevation near glacial border; lower limit rises southward. A-b planes of stones tend to parallel trend of net or polygon . tn pits, stone concentrations usually narrow downwards , te�nating at depths from 0.4 to greater than 1.6 m. Depth to base of stone concentration gene rally increases northward and with increasing altitude . Smaller-scale sorted r..:t.s , etc., are active at higher elevatir>ns throughout the region.

Clark, G. M. , 1�73, Same geomorphic aspects and problems related to the Knox County area, Tennessee, in Geology of Knox County, Tennessee : Tennessee Divisior. of Geology Bulletin 70: Nashville, 'IN, Division of Geology, p. 1-8 . Author describes physiography , then discusses evidence for climatic change , regoliths, historical geomorphology, geomorphic processes, and karst.

Clar�, G. M. , 1984, Periglacial features in the high Appalachians south of the glacial border: CUrrent research; The University of Tennessee : Paleoenvironments, v. 1, p. 85-87 . �thor briefly reviews the occurrence , distribution, and inferred genesis of features believed to be of paleoperiglacial origin.

Clark , G. M. , 1987, Some major topographic and drainage relatior �hips in the North Fork Mountain-Smoke Hole area, Grant and Pendleton c�mties , We st Virginia, in Kite , J. s., ed., Research on the late Cenozoic of the Potomac highlands : SE Friends of the Pleistocene , p. 67-77. Briefly discusse� �� classical geomorphological problems in the area : 1) what is the origin and evolution of transverse water-gap drainage (North Fork Gap ) and 2) how and by what mechanisms have meanders of longitudinal drainage become incised into complexly deformed strata of variable resistance (Smoke Hole Canyon ).

Clark , G. M. , 1987, Stono-related geomorphic effects of the 17-18 June , 1949, rainfall event in the Ridge and Valley province of west Virgin!a: A review, in Kite, J. s. , ed., Research on the late Cenozoic of the Potomac highlands : SE Friends of the Pleistocene , p. 56-62. Briefly describes the storm, hillslope failures, and flooding accompanying the 1949 storm. Debris slides and flows were particularly prominent. Near the crest of North Fork Mountain, one observer reported that the mountain slope was veneered by a continuous sheet of ove rland flow 6 inches thick during height of storm.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 c�ark, G. M. , Ryan, P. T. , Jr ., and Drumm, E. c. , 1987, Debris slides and debris flows on Anakeesta Ridge , Great Smoky Mountains National Park , Tennessee [Extended abstract]: u.s. Geological Survey Circular, v. 1008, p. 18-19. Attempted to find locational and temporal predictors of avalanches. Useful indicators include morpho!ogy, drainage , vegetation, tension cracks in vegetation mat, tree fall scars, and geologic structure. Scar head and scar flank wastage stations are positioned on the ridge to monitor soil and vegetational mat stability. Backwasting of soil and vegetational mats continues at the scar heads. The chute flanks are more stable.

Clark, K. A. , 1976, Bedrock geology and karst development in Grant and Mineral counties, West Virginia [M.S. thesis] : Toledo,OH, University of Toledo , 100 p. Author attempts to determine the structural and stratigraphic factors that control local karst development in the Wills Mountain anticlinorium. Ka rstification processes favor solution in the Tonol�.y rather than the Helderberg formations because of a higher micrite content, a higher total carbonate content, and a higher joint density. The majority of karst features are controlled by stratigraphy rather than by jointing and fracturing. Solutional development is limited to clastic-carbonate geologic contacts, with the majority of karst features restricted to topographically low and gently inclined carbonate strata.

Clark, w. z. , and Zisa, A. c. , 1976 , Physiographic map of Georgia: Atlanta , Georgia Dept . Natural Resources, 1 p. Color map of scale 1:500,000 of physiographic provinces and divisions . Brief descriptions of physiography provided for each.

Cleary, �� . J. , and Conolly, J. R. , 1971, Distribution and genesis of quartz in a Piedmont-coastal Plain environment: Geological Society of America Bulletin, v. 82, p. 2755-2766. Authors study the mineralogical change in river sands as they are transported from the Piedmont to the Coastal Plain. Also study mineralogy of sand in Piedmont soils to ascertain nature of parent material of the river sediments. Show downstream changes as histograms.

Cleaves, E. T. , 1968 , Piedmont and Coastal Plain geology along the Su��hanna aq.1educt, Baltimore t-:> Aberdeen, Maryland: Maryland Geological Survey Report of Investigations , v. 8, 45 p. Geology of a 22-mile section of aqueduct mapped. Where sediments overlie saprolite, at least the upper portion of the saprolite was formed prior to sedimen� deposition. Evidence : 1) extensio� of the saprolite on the Piedmont beneath the Coastal Plain sediments ; truncation of massive and structured saprolite zones by sedimentary deposits; 3) incorporation of saprolite particles into basal sands and gravels; and 4) occurrence of lag gravels at saprolite-sed�ment CC'!ltacts. The lower part of the saprolite may have developed after burial. Contains cross sections .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Cleaves, E. T. , 1973, Chemical weathering and landforms in a portion of Baltimore County, Maryland [Ph.D. thesis): Baltimore, Johns Hopkins University, 185 p. Describes weatherin� of Piedmont rocks and development of saprolite . Notes that in saprolite, up to 60 % of the rock mass may be removed without apparent reduction of the land mass. Although chemical weathering affects all of t�e rocks, shapin0 of the landscape results from mass wasting and f!uvial erosion. Chemical weathering itself lowers the land surface only on serpentine terrane . The DrJdern landscape has been sculptured by mechanical weathering in the lat Miocene to the present . The streams have been entrenched from a pre-Miocene peneplain into bedrock through a pre-existing soil-saprolite sequence , wh ile upland surfaces have remained unaltered.

Cleaves, E. T. , 1974, Petrologic and chemical investigation of chemical weathering in mafic rocks, eastern Piedmont of Maryland: Maryland Geological Survey Report of Investigations, v. 25, 28 p. Microenvironments of chemical weathering were investigated for eight mafic rock weathering profiles by petrologic and chemical methods in the eastern Piedmont of Baltimore and Harford Counties, Maryland.

Cleaves, E. T. , Godfrey, A. E. , and Bricker, 0. P., 1970, Geochemical balance of a small. waterFhed and its geomorphic implicat ions : Geological Society of �rica Bulletin, v. 81, p. 3015-3032. A detailed input-output study of a small forE'sted watershed revealed that chemical weathering is 5 times as effective in removing material than is mechanical erosion. 'nle weathering DrJdel der1ved from study suggests that on a long-term basis approximately

one--ha- � of the watershed erosion is caused by chemical solution of ti:._. � .cate minerals kaolinite, vermiculite, biotite, and ol ; lase.

Cloud, P. E., Jr., 1966, Bauxite deposits of the Anniston, Fort Payne , and Ashville areas of northeastern Alabama : u.s. Geological Survey Bulletin, v. 1199, p. 01-o35. Bauxite, kaolin, and associated unconsolidated sediments in each of three areas appear to fill sinklike depress:ons in unde rlying carbonate rocks of early Paleozoic age . A fossil flora, probably of early Tertiary age , was collect� from lignite lenses in the unconsolidated sediments in two ateas.

Coates, D. R., 1958, Quantitative geomorphology of small drainage basins of southern Indiana (Technical Report no . 10, Project NR 389-042, Office of Naval Research) : New York , Columbia University, 67 p. Morphometric analysis of six small areas in the unglaciuted part of southern Indiana provided data for determination of influence of lithology, percent of unconsumed upland (stage of erosion cycle ), and regional relief upon scale and form properties of thi rd-order drainage basins measured in the field and from topographic maps and air photos .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Cobb, C. , 1893, On the geological history of certain topographical features east of the Blue Ridge : Elisha Mitchell ScientiLic Society Journal, v. 10, p. 94-97 . Author investigated "topographic outliers of the Blue Ridge" in the Piedmont , since referred to as inselbergs. Concluded that these steep-sided hills were the product of wave action at the base of cliffs, acting in the Cretaceous or later. Claimed benches existed at 1000 and 1400 ft elevation.

Cole, w. S., 1934, Identification of erosion surfaces ln eastern and southern Ohio: Journal of Geology, v. 42, p. 285-294 . TWo pronounced upland erosion surfaces are present in eastern and southern Ohio. Below these surfaces strath valleys and strath terraces are found . Correlations with other well known Appalachian surf- 1s are proposed for both the upland and strath surfaces.

Cole , � 1935, Rock resistance and peneplain expression: Journal of Geology, v. 43, p. 1049-1062. The su�face configuration of eastern Ohio and adjacent West Virginia and Kentucky is governed by varying resistance and attitude of strata which have been differentially sculptured during four cyc1 of erosion. The occurrence of rPsistant Mississippian and basa·· �nnsylvanian rocks between weakerks, roc in combination with the JJnl09ic structure, has produced a cuesta and lowland wh: :h domiPate the landscape of eastern Ohio and a portion of KentucY.y. Because of differences in topographic expression and physiographic n• story the cuesta and lowland should not be included in the Kanawha �ection of the Appalachian Plateau.

Cole, w. s., 1937, Development and structural control of erosion surfaces : Journal of Geology, v. 45, p. 141-157. Projected profiles and field observations indicate that there are three major and on< �nor upland surfaces in the Appalachian Plateau of western Pennsylvania and eastern Ohio. Arguments are advanced to prove that these represent erosion surfaces developed under four distinct baselevel controls. The effect of structure upon the development and configuration of these surfaces is considered.

Cole, W. S., 1938, Erosion surfaces of western and central New Yor� : Journal of Geology, v. 46, p. 191-206. The occur�ence of two major erosion surfaces in south-cer tral and western New York is substantiated and a correlation with those of western Pennsylvania and eastern Ohio suggested. A younger sur face and strath are found in the northern portion of western and central New Yo rk, although they are largely concealed by glacial drift. The effect of structure upon the development ard preservation of these surfaces is considered.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Cole, W. s. , 1941, Nomenclature and correlation of Appalachian erosion surfaces: Journal of Geology, v. 49 , p. 129-148 . A correlation of the erosion S\lrfaces of eastern Pennsylvania and adjacent areas with those of western Pennsylvania, eastern Ohio, and southern Nt York is proposed. Thrl�e erosion surfaces and an extensive strath are found in both the ·:astern and western areas. 'lbe Upland surface, c011100n to both reg11.ms , is the only true peneplain. 'lhe younge r surfaces and the straths are correlated by their position below the Upland surfac• !. 'lbe age of the surfaces is considered.

Collier, L and Flint, R. F., 1964, Fluvial se1imentation in Mammoth Cave , Kentuck·•: u.S. Geological Survey Professional Paper , v. 475-D, p. 0141- 0143. Alternating deposition and erosion occur in Mammoth Cave by flooding from the Green River. In two and one half years, nume rous lnw floods deposited 0.5 ft of sediment in the lowest levels. 'lhree high floods reooved that sediment, but caused thinner deposits at higher levels. 'lhe coarsest sediment is deposited in lower parts of the cave .

Collier, C. R. , Pickering, R. J., and Musser, J. J., 1970, Influences of strip mining on the hydrologic environment of parts of Beaver Creek basin, Kentucky, 1955-66: u.s. Geological survey Professional Paper, v. 427-c, p. C1-c77 . Seccion on erosion and sedimentation, p. C31-c46 is most perti nent . Sediment yield went from 25 tons;square mile to 27,000 . Sheet erosion on the gently sloping top of the spoil bank decreased appreciably during the latter part of study period, whereas loss of material by gully erosion increased with time. Erosion of abandoned haul roads also severe , with sediment yields up to 90 tons per acre of road (i.e. , 57, 600 tons/square mile ).

Colman, S. M. , 1983 , Progressive changes in the morphology of fluvial terraces and scarps along the Rappahannock River, Virginia: Earth Surface Processes and Landforms , v. 8, p. 201·-211. Terraces studied were in Coastal Plain. Oldest is no younge r than early Quaternary and the youngest major fill terrace probably correlates with the high sea level of the last major interglacial . Indices of terrace pre3ervation, especially drainage densities and area-to-perimeter ratios, show systematic changes with terrace age . For a given scarp height, older scarps tend to have gentler slopes. Terrace fo�; are preserved for at least several million years and depcdtiona� features such as bars and channels with 1-3 m of relief are �reserved on terraces for about 100,000 yr. Terraces of tl� latter age have slopes of 6-8 degrees where the scarp height is about 5 ln.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Conant, L. C., Black , R. F., an� Hosterman , J. w. , 1976, Sediment-filled pots in upland gravels of Maryland and Virginia: Journal of Research of the U.S. Geological Survey, v. 4, p. 353-358 . Pot-shaped depressions filled with sandy clayey silt are found in "Upland" gravels (previously termed Brandywine ) of probable Miocene age , , '!ar Washington, DC. '!he pots are about 2 m deep and c0111110nly are about as wide . Filling in some pots shows faint stratification paralleling the sides . Strata in the enclosing gravel commonly bend downward and are thinner beside and below the pots. All pots are at gravel surface . Authors suggest pots originated when seasonal frost ir an overlying layer of sandy clayey silt provided a confini�� uppe r layer.

Cooper, B. t-�. , 1944, Geology and mineral resources of the Burkes Garden quadr�.�le, Virginia: Vi rginia Geological Survey lletin,Bu v. 60, 299 p. Author includes good section on geomorphology (p. 205-230 ) Discusse& volume of fan deposits, Blue Ridge escarpment, relative topographic potency of various ridge-makers, surface and subsurface stream capture, effects of structure and lithology on drainage . Sugges•� that the Appalachian region has maintained a perenially matur• .,pography.

Cooper, B . ... , 1961, Geological Guidebook no . 1, Grand Appalachian Excursion: Blacksburg, VA, Virginia Tech, 187 p. Short but pithy sections on surface features and ge�norphology. Discusses origin of Blue Ridge escarpment, rejuvenation of streams, New River straths, drainage evolution, evidence for and against erosion cycles.

Corgan, J. X. , and Parks, J. T. , 1979, Natural bridges of Tennessee : Tennessee Division of Geology, v. 80 , 102 p. Authors describe 36 natural bridges. Majority are in Mississippian-age limestones along the escarpment of the Highland Rim or in Pennsylvanian-age sandstones of the cumberland Plateau. Most bridges can be assigned to one of 7 genetic categories.

Costa, J. E. , 1973, Geomorphic evolution and environmental geology of Western Run watershed, Baltimore County, Maryland [Ph.D. thesis] : Baltimore, Johns Hopkins university, 263 p. A surficial deposits map was constructed, keyed to the predic tion of resi� depth over a given rock unit. A weathering model incorporates mineralogy, topography, and structure into prediction of depth of saprolite . Changing land use has increased runoff and sediment loads to streams by at least four fold. Estimates of volumes of alluvial fill , soil erosion, reservoir sedimentation, and sediment delivery ratios suggest that over one half of the eroded sediment in Western Run is retained as colluvium within the basin.

•

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Costa, J. E. , 1974, Response and recovery of a Piedmont watershed from tropical storm Agnes, ,June 1972: 'jlilater Resources Re search, v. 10, p. 106-112. Despite the magnitude of the flooding {633 cfs/square mile from 60 square miles ) there were no slope failures in the basin. The only modification to the watershed were observed in the lowlands along the main channels. Channe.l widening was the oost spectacular modification. Within one year of the flood, channel cross sections were well along recovery t Mard rre-Agnes dimensions . Large floods in the Piedmont apparently play a minor r�.e i� shaping the landscape, in contrast to the other provinces the Appalachian Highlands .

Costa , J. E. , 1974, Stratigraphic, morphologic, and pedologic evidence of large floods in humid environments: Geology, v. 2, p. 301-303. Discusses evidence of la:ge floods likely to be preserved . Discussion is general in nature, although some ex; les from the �?palachian region are used.

costa , J. E., 1975, Effects of agriculture on erosion and �edimentation in the PiediOOnt province , Maryland: Geological Society of America Bulletin, v. 86 , p. 1281-1286 . A study of surficial deposits has made it possible to construct a balance equation of sediment production and deposition since erosive agricultural land use began in the 1700's. Truncated upland soil profiles imply about 0.15 m of soil erosion. Reservoi r sedimentation rates imply that 34 percent of the eroded sediment has been carried out of the system, the rest remaining as alluviu... in the upper 1 m of flood plains and as colluvium and sheetwash deposits on hi:i.lslopes. About 14 percent of the estimated erosion is stored on flood plains and 52 percent on hillslopes. Evidence suggests that since the decline of agriculture in the early 1900's, small upland tributaries have adjusted to decreased sediment loads by entrenchment into and erosion of sediment deposited since the initiation of colonial agriculture.

Costa, J. E., and Cleaves , E. T., 1984 , The PiediOOnt landscape of Maryland : A new look at an old problem: Earth Surface Processes and Landforms, v. 9, p. 59-74. The Piedmont upland of Maryland has been variously interpreted as a peneplain, a series of peneplains, and a landscape in dynamdc equilibrium. These different perspectives of landform evolution are related to different scales of time and space . Both equilibrium and episodic features can be recognized in modern landscape . An equilibrium condition is suggested by adjustmer.t of 1st and 2nd order streams to rock structure and lithology, altitudinal zonation of rock types around gneiss domes, correlation of lithology with overburden thickness on uplands, and correlation of secondary mineral assemblages with drainage and slope . The long-term episodic character of erosion is suggested by clastic wedges on the adjacent Coastal Plain, and by an upland of low relief that truncates non-carbonate rocks of different lithologies, for example.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Costain, J. K. , Bollinger, G. A. , and Speer, J. A. , 1987 , Hydroseismicity - A hypothesis for the role of water in the gene ration of intraplate selsmicity: Geology, v. 15, p. 618-621 . A new hypothesis termed hydroseismicity suggests that in crustal rocks with fracture permeability, natural increase in hydraulic head caused by transient increases in the elevation of the water tat>l e in recharg� areas of groundwater basins can be transmitted to depths of 10-20 km and thereby trigger earthquakes. Note that each of the four major seismogenic zones of the Southeast is inferred or known to be t.nderlain by rifted cmst. Likewise , major rivers flow through these areas . Suggest that the roost probable seisroogenic intraplate crustal volt�s are at the intersections of 1) higher fr�cture permeability that is characteristic of rifted crust and 2) major river ba�ins with a gravity-driven subsurface groundwater flow regime that can provide an adequate sour�e of meteoric water from recharge areas to the upper crust. Figure 2 shows maj01: rivers, historical seismicity, and instrumentally located epicenters of Southeast .

Craig, F. G. , 19�9, A simulation model of landscape erosion [Ph.D. thesis]: university Park, Pennsylvania State University, 536 p. A stochastic model of the development of landforms is formulated using the Markov property. 'Ibis model is then implemented in a Monte carlo computer simulation which includes subroutines for reconstructing theoretical surfaces at arbitrary elevations above the present . The model simulates erosion and tests the derived surface to determine how closely it corresponds to the present-day surface. '!be model is applied to the Appalachians of Pe�sylvania.

Craig, R. G. , 1982, The ergodic principle in erosional models, in Col in, E. T. , ed., Space and time in geOillOrphology: London , Allen & Unwin, p. 81-115. Author discusses a landform simulation model and applies it to the Appalachians of Pennsylvania. On a grid, elevation and lithology were recorded for the example areas, and the model applied.

Cranford, s. L. , Bobyarchick, A. R. , Pavlides, L., and Wier, K. , 1982 , Stream control by foliation, joints, and folds in the Rappahannock River drainage system near Fredericksburg, Virginia: u.s. Geological �urvey Miscellaneous Investigation Series, v. I-1285, 1 p. Most tribo.Jtaries to the Rappahannock in the study area follow the prevalent northeast-trending foliation in ti1e area. Joints are of secondary importance, locally controlling northwest flowing, bedrock-incising streams .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Crawford, N. �., 1978 , Subterranean stre&� invasion, condui t cavern develo�ment and slq;>e retreat: A surface-subsurface erosion model for areas of c:::rbonate rock overlain by less soluble and less permeable caprock [Ph.D. thesis]: wo rcester, MA, Clark University, 505 p. Mode � states that conduit cav�s form by subterranean invasion of surface streams :ong retreating caprock escarpments which result from faster chemical erosion of uuderlying carbonates. Some of th� points in the model include : 1) Invasion occurs near contact between imperrueable caprock and underlying carbonates as caproLk streams, highly aggressive to CaC03 , begin to flow th��ugh caroonatef. to resurgences near escarpment base; 2) cav es are enlarged almost exclusively by the corrosion and corrasion of swaliet streams , particularly during floods; 3) A subsurface stream takes a "stair step" route down the escaq:ment due to the presence of thin, resistant, impermeable layers of shale, sandstone , and chert between the limestone ; 4) These resistant , impermeable strata act as base levels for cave development.

Crawford, N. C., 1979 , Karst hydrogeology of the Cumberland Plateau escarpment in the Lost Creek Cove and Grassy Cove areas of Tennessee: Safford Centennial Society Field Trip, Fall 1979: Bowling Green, KY, Western Kentucky University, 49 p. Testsmodel that conduit caves formby subterranean invasion of surface streams along retreating caprock escarpments which result from faster chemical erosion of underlying carbonates. See Ph .D. thesis sUlllllary for nue details.

Crawford, N. C. , 1979, The karst hydrogeology of the Cumberland Pli'.teau escarpment of Tennessee , Part I: Subterranean stream invasion, condu1t cavern development, and slope retreat in the Lost Creek Cove area, White County, Tennessee .: Cave and Karst Studies Series (western Kantucky University) , v. 1, 75 p. Model states that conduit caves form by subterranean invasi�n of surface streams along retreating caprock escarpments which result

from faster chemical erosion of underl�-�"lg carbonates. See Pl'. . l'. abstract for more details.

Crawford, N. � •• 1979, The karst hydrogeology of the Cumbe rland Plateau escarpment of Tennessee, Part II: Karst valley development and t�e headward advance of the Sequatchie valle { ;n the Grassy Cove area. CUmberland County, Tennessee : C.. 1e .u.d r_, . st Studies Series (�c;tern Kentucky University) , v. 2, 51 p. Grassy Cove , the hollowed-out cent�r of & large �ticline, has flanks that protrude 300 m above the Ple-;_eau and 400 m abcve the

floor of the cove . Author tests model w' j r :; <:t:ates that �{ ·ndui t caves form by subterranean invasion of surface stre�ms along retreating caprock escarpments which result from fa.;ter ••• emical erosion of underlying carbonates. See Ph .D. abstract for �re details.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Crawford, N. C., 1980, The karst hyd rogeology of the CUmberland Plateau escarpment of Tennessee, Part III: Karst valley development in the Lost Cove area, Franklin Countv, Tennessee: cave and Karst Studies Series (western Kentucky university) , v. 3, 21 p. Lost Cove is a large karst valley located in thr1 sout;1ern portion of the CUmberland Plateau. Author tests model whic'1 states that conduit caves term by subterranean invasion of surface streams along retreating caprock escarpments Which result from faster chemical erosion of underlying carbor �es. See Ph .D. absttdct for mre details.

Crawford , N. C. , 1980, The karst hydroge0logy of the Cumberland P�ateau escarpment of Tennes�ee, Part IV: Erosional processes associated with subterranean stream invasion, conduit cavern development, and s.1.ope retreat: Cave and Karst Studies series (western Kentucky university) , v. 4, 152 p. Author tests model which states that colk.tat caves form by subterranean invasion of surface streams along retreating caprock escarpments which result from faster chemical erosion of underlying carbonates . cave systems in the Grassy Cove area were mni to red for 15 mnth'! . Findings included: 1) caprock streams are always ag�r&ssive to limestone ; 2) Percolation input is always supersaturated with calcium carbonate on joining the cave system; 3) A direct correlation exists between aggressivity and discharge for the swaPet input and ri.sing output .

Crawford, N. c. , 1981, Karst flooding in urban areas : Bowling Green, Kentucky, in Beck , B. F., ed., Eighth International Congress of Speleology, Proceedings: Huntsville, Alabama, NSS, p. 763-765. Bowling Green depends upon the subsurface Lost River and its tributaries to serve as natural storm sewe rs. Since it is prohibitively expensive to build storm sewers in mst karst areas, restricting development in sinkholes which flood by a combination of zoning and stormwater retention basins appears to be the mst effective method of dealing with sinkhole flooding. Retention basins are also effective in reducing urban stormwater pollution of karst aqui fers.

Crawford, N. C. , 1981, Karst valley development and the headward advance of the sequatchie valley of Tennessee along the Sequatchie anticline, in Beck, B. F., ed., Eighth International Congress of Speleology, Proceedings : Huntsville, AL, NSS , p. 814-819. caprock streams flowing down dip off the Sequatchie antj cline often breach the silicious cdprock and invade the underlying carbonates. A conduit cave is formed by the gressiv ag e waters of an invading stream as it flows from its swallet to a rising at the head of the Sequatchie valley. Slope retreat by sapping proceeds in all directions away fran the site of the initi�l invasion, resulting in large karst valleys completely surrounded by caprock . The anticlinal mountain is first reduced to karst val�eys which are then assimilated into the Sequatchie valley as it advances headward up the Sequatchie anticline . Thus subterranean stream invasion, conduit cavern development, and the growth of karst valleys play a major role in changing anticlinal muntains into anticlinal valleys .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Crawford , N. C. , 1982 , Hydrogeologic problems resulting from deve lopment upon karst terrain, Bowling Green , fCentucky : Guidebook pr�:·rared for Karst Hydrogeology WOrkshop , August 31-September 3, 1982, Nashville, Tennessee , u.s. Environmental Protection Agency: Bowling Green, KY, We stern Kentucky university, 34 p. Author discusse3 karst hydrogeology, sinkhole flooding, and pollution of karst aquifers. Fou rteen field-trip stops illustrate these problems.

Crawford, N. C. , 1982 , Karst hyd rogeology of Tennessee : Guidebook prepared for karst hydrogeology workshop , August 31-Sept�::;:::._"'er 3, 1982, Nashvi lle , Tennessee , U.S. Envi ronmental Protection Agency .: Bowling Green , KY, western Kentucky university, 102 p. Author proposes and tests model which states that conduit caves form by subterranean invasion of surface streams along retreating caprock escarpments which result from faster chemical erosion of underlying carbonates. A shortened version of Ph .D. thesis .

Crawford, N. c. , 1984, Karst landform development along the Cumberland Plateau escarpment of Tennessee, in LaFleur , R. G. , eel. , Groundwater as a geomo�1ic agent : Boston, Allen & unwin, p. 294-339. Author investigated the relationship between subterranean stream invasion , slope retreat, topography, subsurface hydrology, conduit cavern development, stucture, and stratigraphy . An eroDion model was hypothesized and tested. This model states that conduit caves form by subterranear. invasion of surface streares along retreating esca�nts which result from faster chemical e.·osion of underlying carbonates.

Crawford, N. C. , 1985, Groundwater flow and geologic structure , Lost Creek groundwater basir. : Bowl ing Green, KY, Cente r for cave and Karst Studies, 1 p. Map shows groundwater basins, streams and lakes, stream sinks , gauge sites , hypothesized and mapped subterranean stream routes , dye traces, springs , karst windows , and structure contours drawn on top of the Chattanooga Shale.

Crawford, N. c. , 1985, Groundwater flow routes, Lost River grow1dwater t�sins : Bowling Green, KY, Cente r for cave and Karst Studies, 1 p. Map shows groundwater basins , streams and lakes, stream sinks , gauge sites, mapped and hypothesized subterranean stream routes , dye traces, springs, and karst windows .

Crawford, N. C. , 1986 , Karst hydrologic problems associated �ith urban development : ground water contamination, hazardou� fumes , sinkhole flooding, and sinkhole collapse in the Bowl ing Green area, Kentucky: Field guide prepared for Nl'iWA symposium, OCtober 28-30, 1986, Bowling Green, KY: Bowling Green, Ki, western Kentucky university, 86 p. Author discusses problems of fumes in caves, sinkhole flooding , karst aqui fer pollution, and sinkhole collapse . Twenty-one stops illustrate these problems .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Crawford, N. c. , and Groves , c. G. , 1984 , Storm water drainage wells in the kar:::.l areas of Kentucky and Tennessee : Bowling Green , KY, r2nt.er for Cave and Karst studies , 52 p. A total of 572 wells were located and investigated, with 444 occurring in Bowling Green . Storm-water �rainage wells often reduce and in some cases eliminate sinkhole flooding, Lu t there are seve ral potential �roblems : 1) low capacity; 2J clogging from d�bris and sediment ; 3) sinkhole collapse ; 4) pollution from urban storm wa ter runoff ; 5) mixing of groundwater between aqui fers.

Crickmay, C. H., 1937 , The later stages of the cyde of erosion: Geological Magazine, v. 70, p. 337-347. Author points out weaknesses in the theory of the cycle of erosion, and argues for his panplair:ation t.'leory; panplains are fnrmed of floodplains joj -.ed by thei r own growth. Ir. the discussion he uses examples from the Af"'Cllachians , among other places .

Crickmay, G. F., 1935, Granite pedestal rocks in the southern Appalachian Piedmont : Jcurnll of Geology, v. 43, p. 745-758 . Pedestal rocks of granite, commonly associated with resi�Jal boulde rs, occur at many places. Rocks are essentially homogeneous i� composition but exhibit marked contrast in weathe ring of the cap and the sha�t. Granular disintegration initiated by expansion through hyd ration is the dominant process involved . trjd ration is the dominant process involved . Hydration is at a maximum on lower slopes where there is some protection from di rect rats of the sun and where evaporation is at a minimum.

Cronce, R. C. , �� Ciolkosz , E. J. , 1986 , Soil development in periglacial frost wedg� casts of central Pennsylvania [Absttact]: American Quaternary Association, Program and Abstracts of the Ninth Biennial Meetirq, v. 9, p. 125. Objectives were 1) to document the location , size, ar.d 1>hape of c numbe r of wedge fcrms in the area; 2) to determine tht:: chbrar.:teristics of the soil profiles developed within the �<:dge forms , and 3) to use this information to estimate the history and climatic conditions at time of development .

�rowl , G. H. , 1971 , Pleistocene geology and w.consolidated deposits of the Delaware Va lley, Matamoras to Shawnee On Delaware, Pennsylvania: Pennsylvania Geologic Survey, 4th series, General Geology r.e port, v. G60. On p. 12-14, author discusses hillslope depo5its beyond the Wisconsinan terminal moraine, including shale-chip colluvium, which he calli> "sharpstone colluvium" .

Crowl , G. H. , 1980, WOOdfordian age of the Wisconsin glacial border in northeastern Pennsylvania: Geol�J, v. 8, p. 51-55 . Radiocarbon dates beyond the Wisconsin glac�al border are comtemporary with or sCIILciWhat older than those along the border, indicating that mass movement in this extraglacial region probably ceased, al lowing organic sediments tc accumulate , about thP. same time that ice began to retreat . The ice sheet pr Jbably began to retreat about 15,000 B.P.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 CUllison, J. s. , 1936 , Subte rranean and surface stream pi racy of Gap Creek and its tributary [Abstract ): Geological Society Proceedings for 1935, v. 1935, p. 73. Four miles south of Cumberland Gap, 'IN, the area of' its source , Gap Creek, enters a subterranean channel, through which it flows for a di stance of at least 1250 ft . The creek emerges at an elevation of about 100 ft lower . The decreas� in elevation of the lower portion of G.:lp Creek has rejuvenated the main tributary of lower Gap Creek , to such an extent as to cause the surface capture of a stream which was originally a tri�t3ry of uppe r Gap Creek .

CUnningham, R. L. , and Ciolkosz , E. J., 1984, Soj ls of the northeastern Un ited States: Pennsylvania 3tate University, Agri�ultural Experiment Station Bulletin, v. 848 , 47 p. Authors provide brief d�scription of soil classification, then provide chapters on entisols, inceptisols, alfisols, ultisols, spodosols, histosols. There ara also chapters on uses and interpretation, and on general soil-map characteristics.

Curn ingham, R. L. , Ciolkosz , E. J. , Matelski , R. P., Petersen, G. w. , and Pennock , R. , Jr. , 1974, Characteristics, interpretations , and uses of Pennsylvania soils developed from colluvium: Pennsylvania State University Agricultur 1 Expe riment Station Progress Report, v. 344, 49 p. Authors discuss soil series that have developed in colluvium. All are heterogeneous , and most have a fragipan horizon that typifies Pennsylvania soils developed in transported parent materials.

CUnningham, R. L., Lipscomb, G. H. , Petersen, G. W. , Ciolkosz , E. J. , Shipp, R. F. , Pennock , R. , Jr., Cronce , R. c. , and Sacksteder, c. J. , 1983 , SoilG of Pennsylvania: Characteristics, interpretations , a:.d extent : Pennsylvania State University Ag ricultural Experiment Station Progress Report, v. 380 , 135 p. only 9 pages of text , in which soils are di scussed in a gene ral fashion . Mainly contains mapping-unit legends, by county.

Currens , J. c. , 1981 , Speleogenesis models for the Mammoth Cave region , � their u�e as predictive tools for southern Toohey Ridge , Hart and Barren counties , Kentucky, in Beck , B. F. , ed ., Eighth International Congress cf Speleology, Proceedings : Huntsville , AL, NSS , p. 75-78. Mode ls which seemed to best explain the trend and location of major passages in northern Toohey Ridge are used to synthesize predictions of major passage locations and trends in southern Toohey Ridge .

Currens , J. C. , and McGrain, P. , 1979 , Bibliography of karst geology in Kentacky: l

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 D'Appolonia, E. , Alperstein, R. , and D'Appolonia, D. J., 1967 , Behavior of a colluvial slope : Journal of Soil Mechanics, Foundation Engineering Division, American Society of Civil Engineers, ..,. 93, p. 447-47::: . Radiocarbon dating showed that movement of the colluvium into the valley bottom occurred at least 40,000 yr ago . The factor of safety against a drained failure prior to construction was 1.0 using the residual slope parameters. However, field observations indicated that the slope had not moved recently. This, together with laboratory test results and analysis of actual slides, suggests that "healing" of the slickensides has occu::red, although the mechanism of "healing" i:; not known .

Dallmeyer, R. D., 1975, Incremental 40Ar/39Ar ages of biotite and hornblend from retrograde basement gneisses of the southern Blue Ridge : American Journal of Science , v. 275, p. 444-460. Author outlines an erosional h.�tory of the Blue Ridge since Ordovician times. says erosion rate was 100 mm/1000 yr up to the Triassic, and slower thereafter, par�icularly in the cretaceL�S and Cenozoic.

Darmody, R. G. , and Foss, J. E., 1�82 , Soil-landscape relaLionships in the Piedmont of M��land : Soil Science 5ociety of America Journal , v. 46, p. 538-592 . Soil series of particular interest were the Chester, Glenel� . and Elioak series of Typic Hapludults. Results indicate that the Elioak soil is a relict pal�osol. A stone line separating strongly weathered Elioak soll material from silty overburden was revealed in several excavations. Comparisons with known and radiocarbon-dated loess deposits on the eastern shore of Maryland indicate that the silty overburden on the Piedmont is loess which was deposited after 10,520 plus or minus 240 yr B.P. Fig. 4 shows idealized sequence of landscape evolution and pedogenesis in the Piedmont of Matyland.

Darton, N. H. , 1894, Outline of Cenozoic histo�J of a portion of the Middle Atlantic slope : Journal of Geology, v. 2, p. 568-587. Author states that it is now ve�:i clearly recognized that-. the

Piedmont plateau is a peneplain of Tertiary age ••• In the P1edmont region, the plain has been deeply trenched by drainageways , but

wide areas are preserved in the divides ••.[Th is penep�ain] extends ove r the Piedmont plateau to the foot of the mountains and thei r g�rges. Figure 5 is map of the Middle Atlantic s:Jpe, indicating the conditions in the time of post-<::oll.unbi<>. maxiDnllll uplift. Also shown is the nature of �, e deformation of the Tertiary peneplain in 100-foot contours and the present extent of Lafayette deposits.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Darton, N. H. , 1950, Configuration of the bedrock surface of the District of Columbia and vicinity: U.S. Geological Survey Professional Paper , v. 217, 42 p. Describes bedrock configuration in washington, DC area. The southeasterly slope of the bedrock is in gene ral very regular at a rate of 100-150 ft;mi , but there are local variations in di rection and amount . Where data are closely spaced they reveal low mounds and ridges and shallow valleys which had been developed as surface features on the old pre-Cretaceous rocks upon which the beds of the Potomac group were deposited. Possibly also some faulting or even flexing has taken place .

Davies, W. E., 1951 , Mechanics of cavern treakdown: NSS Bulletin, v. 13, p. 36- 43. Author provides mechanical analysi� or �avern breakdown, using examples from We st Virginia caves.

Davies, w. E., 1953, Geology of Pennsylvania caves: NSS Bulletin, v. 15, p. 3-9 . Discusses in general terms the occurrence of caves in Pennsylvanj a,

Davies, w. E., 1957, Erosion levels in the Potomac drainage system and their ralation to cavern development : Speleo Digest, v. 1957 , p. 2.32-2.36. In the area drained by the South Branch and its tributaries, nine distinct erosion levels are apparent . Five of these are peneplain surfaces high above the present drainage . The other four are Pliocene-Pleistocene terraces directly related to present drainage . Cave levels develJp in response to the current erosion level . Evidence - levels in Shenandoah Valley ca�es clos�ly correspond to terraces of the nearby rivers and are horizontal in spite of the complex structure of the limestones .

Davies, W. E. , 1960, Origin of caves in folded limestone : NSS Bulletin, v. 22, p. 5-18. Author notes !ive features that bear on origin: 1) caves generally have unifonn gentle slope independent of rock structure ; 2) many caves have uniform levels that �re uniform within a region; 3) intervals between passage levels correspond closely to terrace levels of surface streams; 4) major caves are along large valleys ; 5) passages decrease in size and become more nume rous in the part of the cave a�y from major surface valleys . Then propounds model for cavern development .

Davies, W. E., 1964 , The geologic setting, in Douglas, H. H. , ed . , Caves of Virginia: Falls Church, v.A, Vi rginia Cave survey, p. 15-28. Figure 2 shows karst areas in Virginia. Author discusses stratigraphy of limestone units in Virginia. Table 2 lists size and location of larger dolines in southwest Virginia .

Davies, w. E., 1968 , Physiography , in Mineral resources of the Appalachian region, u.s. Geological Survey Professional Paper 580 , p. 37-48. Author briefly describes physiography and cave rns of Appalachians . Figure 10 shows caves in the Appalachian region.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Davies , w. E. , 1976 , Weathering processes and natural hazards in the Blue Ridge and Piedmont , northwestern Virginia : Eighth Annual Virginia Geology Field Conference , October 23, 1976 : Virginia Geology Field Conference , 12 p. Mainly a road log. Describes boulde r streams , landslides, terraces , 200 ft of residuum at Crimora mine .

Davies , W. E., and LeGrand , H. E. , 1972 , Karst : Important kars� regions of the Northern He�sphe re , in Herak , M. , and Stringfield , v. T., eds. , Important karst regions of the Northern Hemisphere : New Yo rk , Elsevier, p. 467-505. On p. 481-501, authors describe occurrence and nature of karst in the Appalachien region. Figure 6 shows Appalachian karst areas .

Davis, J. D. , 1982, Karst geomorphology of uppe r Sinking Cove , Franklin County , Tennessee [M.A. thP.SlS] : Athens , Georgia, Unive rsity of Georgia, 175 p. A multiple-aqui fer karst hydrologic system, with minor surface components , is organized into a central trunk channel . Geologic controls are responsible for the localized production of paraphreatic flow conditions , surface resurgences , and erosional base levels above aquitards, and the preference for joints in groundw�ter routing. Evidence from caves indicates that the present hydrologic system has evolved from similar systems in the past . Vadose condui t flow conditions appear to dor..inate cave development histories, except above aquitards, where paraphreatic flow has played a role .

Davis, w. M. , 1888 , Geographic methods in geologic investigations : National Geographical Magazine, v. 1, p. 11-26 . Discusses the importance of the Appalachians in the development of American geomorphology.

Davi s, w. M. , 1889, A river pi rate : S�ience , v. 13, p. 108-109 . Describes a case of river pi racy.

Davis, w. M., 1889 , The rivers and valleys of Pennsylvania : National Geographical Magazine , v. 1, p. 183-253. The famous paper in which Davis lays the groundwork for his geographical cycle, and also expounds an intricate theory of drainage evolution for the Appalachians of Pennsylvania.

Davis, W. M. , 1889, Topographic development of the Triassic formations of the Connecticu� valley: American Journal of Science , v. 37 , p. 423-434 . D�scusses the manner in which modern drainage has developed from the co·lsequent drainage of the Triassic. In this paper Davis coins the ""� rd "peneplain" .

Davi s, w. ft. , 1890, The rivers of northern New Jersey, with notes on the classi fication of rivers in gene ral : National Geographical Magazine, v. 2, p. 81-1.10 . D: scusses drainage evolution in New Jersey and its relationship to erosior. cycles .

Davi s, W. M. , 1891 , The geologic dates of origin of certain topographic forms on the Atlantic slope of the United States : Geological Society of Amer�ca Bulletin, v. 2, p. 545-581. Di scusses probable ages of different erosion surfaces .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Davis, W. M. , 1892, The Appalachian Mountains of Pennsylvania: Goldthwaite's Geogr-r�ical Magazine, v. 3, p. 343-350 .

Davis, W. M. , 1892, .ne folds of the Appalachians : Goldthwaite's Geogrrphical Magazine, v. 3, p. 251-255.

Davis, W. M .. 1.892, On the drainage of '"lnsylvanian Appalachians : Boston Society of Natural History, Procee v. 25, p. 418-420 .

Aut:.c-- .... ates that whether the , _ rs of Pennsylvania wer� or ..ginally ! :equent or antecedent, tl "ir present courses cannot be explained css the persistence of their r"ll :�:1t original courses, but only by regarding them as having char,�� from their original positions in the p�ocess of adjusting themselves to the structures over which they flow.

Davis, w. M. , 1893 , The Osage River and the Ozark uplift: Science , v. 22 , p. 276-279 . Davis discus&es lines of evidence that level uf Missouri has changed since its Paleozoic emergence , and that the last uplift resulted in streams being cut in the denuded surface of the region.

Davi s, w. M. , 1895, The physical geography of southe rn New England , in The physiography of the united States [Monograph I 1 : Wa shington , DC, National GPographical Society, p. 269-304 . Topics include the upland of southern New England ; the valleys in the upland; review (the upland serves as the type of a peneplain, now uplifted and well �dvanced in a second cycle of denudat · '11 ); the glacial invasion; and the coast line.

Davis, w. M. , 1896, April recess excursion in the middle Sus .ta: Science , v. 3, p. 786-787 . Object of excursion was to study the deflected tributaries of the Susquehanna in union and Snytie r counties, PA , and to determine their !.:earing on the hypothesis that the Susquer:mna was supe rposed b:' flood plaining on the two synclines of Pocono sandstone in Dauphin county at a late stage in the Cr�taceous cycle of denudation.

Da1is, w. M. , 1897, The Triassic Formation of Connecticut : u.s. Geological �urvey Annual Report, v. 18 , p. 1-192 . Part III, "Denudation" , on p. 144-184 is pertin�nt . Di�cusses gene ral principles of land sculpture , cycles of denudation, the initial form of monoclinal faulting, initial drainaye of the faulted monocline, changes from initial to existing drainage , the Cretaceous peneplain, relation of trap ridges to the peneplain, subae rial origin of the peneplain, adjustment of streams to structures, geol01ical date of the peneplain, possible superposition of certain stre�ns , uneven uplift of the peneplain, Tertiary dissection of the upl ift peneplain, effect of faul ts on trap ridges, etc .

Davis, w. M. , 1899, The peneplain: Aoaerican Geologist, v. 23 , p. 2( 7-239 . In discussing the peneplain concept , Davis points to the Piedmont of Vj rginia as an example of a better-preser1ed feneplain. Also refers to other parts of the Appalachians .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Davis, w. M. , 1902 , River terraces in New England : Bul letin of the Museum of Comparative Zoology, Harvard College , Geological Series V, v. 38, p. 281- 346.

Davis, W. M. , 1902 , 1 terraces of the Westfield River, Mass .: American Journal of Science , v. �4, p. 77-94. Davis dis�sses several theories of terrace formation, using terraces of the Westfield River as examples .

oav: ·, w. L, 190':1, '111e stream contest along the Blue Ridge : Geographical �ociety of fhiladelphia Bulletin, v. 3, p. 213-244. The Blue Ridge escarpment results from the reduction of the 1nd surface to a relatively low level by the headwaters of the sLort Atlantic rivers, whose drainage area therefore lies a� a lower level than that of the larger west-flowing rivers of the Mississippi system. '111e escarpment occurs where the Atlantic streams are undercutting the uplands of the Miss. system. Residual mountains rise over the rolling uplands of the Atlantic rivers and ove r the rolling highlands of the Mi ss. River. Kings and Pilot mountains are examples of the first, and Mount Mitchell and Roan mountains the second . Grandfather Mountain stands on the escarpment .

Davis, w. M. , 1906, rncised meandering valleys : Geographical Society of Philadelphia Bulletin, v. 4, p. 182-192 . Mentions examples from the Appalachians in discussing the processes of incised meandering valleys .

Davis, w. M. , 1906, The physiography of the Adirondacks (formation of scarps ): Science , v. 23, p. 630-631.

Davis, W. M. , and Wood , J. W. , Jr., 1890, The geographic development of northern New Jersey: Boston Society of Natural History Proceedings, v. 24 , p. 365- 423. The Highland plateau is an elevated and faintly tilted peneplain of denudation, dissected since its elevation by numerous valleys . The same peneplain determines the crest lines of Kittatinny mountain and of the many simi lar ridges of Pennsylvania on the west, and of the Triassic trap ridges on the east. It may be seen descending below sea-level where the Cretaceous beds lie on it below New Brunswick. Most of the streams that have opened valleys in the Highland portion of the peneplain are simply revivals of old streams of an earlier geographic cycle; in the Triassic area, however, many streams have been supe rposed from Cretaceous strata .

Deike, G. H. , III, and White, W. B., 1969 , Sinuosity in limestone solution conduits: American Journal of Science, v. 267, p. 230-241. cave passages with sinuous patterns are compared with the meander belts of surface streams. TWo types of non-linearity were found : �n angulate form generated by water flow downa hydraulic gradient diagonal to a rectangular joint set and a curvilinear form with sweeping S-bends apparently related to meanders in surface stre�. Relationship between ave rage bend spacing and channel width is similar to that for alluvial rivers.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Deike, R. G. , 1969 , Relations of j .ntir.g to orientation of solut..!.on cavities in limestones of central Pennsylvania : American Journal of Science , v. 267, p. 1230-1248. Segments of 26 caves were ("1unulatet1 by footage to l£ termine statistically preferred orienta c· •• r �sults show caves develop more footage parallel to the stt�k. f � more abundant l .actures.

These most abundant fractures are mair1.� ·tical strike joint · e�· d .1 steeply dipping bedding planes, · 1.cJ ' 't parallel both t0 t�e anticlinal axes and down-valley water il.o-..·.

Delcourt, H. R. , and Delcourt, P. A. , 1985, Quaternary palynology and vegetational history of the southeastern Un ited States, in Bryant, v. M. , Jr., and Holloway, R. G. , eds. , Pollen records of late-Quaternary North American sediments : Amer. Assoc . of Strat. Paly. Foun., p. 1-37 . Authors present a short summary of palynological research in the Southeast, document the onajor radiocarbon--di.ted palynological sequences and literature , describe the modern pollen-vegetation relationships for important tree taxa , characterize the vegetational history for the past 20,000 yr, and indicate key problems for future research in Quaternary paleoecology of the region.

Delcourt, P. A. , 19aO , Quaternary alluvial terraces of the Little Tennessee River valley, east Tennessee: University of Tennessee Department of Anthropology Report of Investigations , v. 29, p. 110-121 , 175-212. Nine sets of river terraces were mapped along the Little ·rennessee River. Trenching at five locations allowed descriptions of weathering profiles and, for Tl and T2 , radiocarbon dates.

Delcourt, P. A. , 1985, The influence of late-Quaternary climatic and vegetational change on paleohydrology in ungl.aciated eastern North America: Ecologia Mediterranea , v. 11 , p. 17-26 . Fossil-pollen assemblages from lacustrine sites across eastern North America have been used to characterize the nature of late-Quaternary climatic change and vegetational development . Lacustrine sedimentation patterns demonstrate paleohydrological response to changes in average climatic and vegetation conditions. Between 35 and 40 degrees north, high rates of sedimentation in lakes between 20 , 000 and 12,500 yr B.P. occurred under cool , moist climatic conditions north of the mean winter position of the Polar Frontal zone . During the Holocene, sedimentation rates slowed, reflecting increased seasonality and variability in precipitation.

Delcourt, P. A. , and Delcourt , H. R. , 1981 , Vegetation maps for eastern North America: 40,000 YR B.P. to the present, in Romans, R. C., ed ., Geobotany II: Plenum Publishing Corp. , p. 123-165. Based on radiocarbon-dated pollen diagrams from 100 localities across eastern Canada and the eastern u.s. , the paleovegetation distribution of eastern North America is mapped for 40,000 yr B.P. , 25,000 yr B.P., 18,000 yr B.P. , 14,000 yr B.P. , 10 ,000 yr B.P., 5,000 yr B.P. , and 200 yr B.P.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Delcourt, P. A., and Delcourt, H. R. , 1984, Late Quaternary paleoclimates and biotic responses in eastern North America and the wester� �orth Atlantic Ocean: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 48 , p. 263- 284 . A series of maps depicting chan �es i.n inferred bour :ies C'f predominant airmasses durin the late 0' '\ternary are b.. �'"" upor. paleoclimatic interpretation of paleoveg_.:at:io n r.aps fc..: eastern North America, � CLIMAP maps of winter sea-surface temperatures for the western North Atlantic Ocean.

�!court, P. A. , and Delcourt, H. R. , 1985, Field trip 7: D-.tm.mic Quaternary landscapes of East Tennessee : An integration of paleoecology, geomorphology, and archaeology, in Woodwa rd, N. B. , ed., Field trips in the southern Appalachians, SE-GSA, March, 1985, u. Tennessee Del?Cirtment of Geological Sciences Studies in Geology: Knoxvi lle , University of Tennessee , p. 191-220. Road log for 9 stops in the Great Smoky Mountain area. Topics include paleoclimate, paleovegetation, periglacial features, terraces of the Little Tennessee River, and pollen sites. Figure 4 is a plot of patterned-ground elevation against latitude .

Dennis, H. w. , 1971 , The pre-recent sediments and erosion surfaces of the Georgia Piedmont [Ph.D. thesis]: Athens , �. University of Georgia, 161 p. Author describe� colluvium, sands, stone lines, and other deposits, many of them relict, on the Georgia Piedmont . Also de scribes field evidence for remnant erosion surfaces.

Dennison, J. M. , and Johnson, R. w. , Jr., 1971, Tertiary intrusions and associated phenomena near the Thi rty-Eighth Parallel fracture zone in Virginia and West Virginia: Geological Society of America Bulletin, v. 82 , p. 501-508 . Authors note that Wright (1925) mapped the Schooley erosion surface in this area, and had noted that the uplift of this peneplain was located along the Alle�heny front in the eastern part of west Virginia, with its greatest elevation in the area around Durbin (Pocahontas Cty) . Authors note that this maxiliiUIIl uplift is remarkably close to the Eoc

Denny , C. s., 1936, Periglacial phenomena in southern connecticut : American Journal of Science , v. 32, p. 322-342 . Author describes deformation of underlying beds near Stratford, whLch he attributes to Pleistocene frost action .

Denny , C. S., 1951 , Pleistocene frost action near the border of the Wisconsin drift in Pennsylvania: Ohio Journal of Science , v. 51, p. 116-125. Author describes rubble slopes, blockfields, and patterned ground just beyond the Wisconsin drift margin. Notes that the surficial mantle becomes th inner and less continuous as one goes away from the drift border, and slopes become steeper.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Denny, c. s., 1955, surficial geology and geomorphology of Potter county, Pennsylvania: u.s. Geological S�rvey Professional Paper, v. 288 , 72 p. Describes ·1rf.:cial geology of area just outside jrift margin, as well as glacial de.JOsits themselves . IncluJ� . extensive discussion of periglacial JepositE Within th1s L �lication is a section by Denny and J.C. Good1 :� on microrelief resulting from fallen trees. They conclude that so1l profiles within the upper 2-3 ft of the surface may not be more than a few hundred years old. This process may also produce rubbly material similar to periglacial deposits .

Denny, c. S., 1982, Geomorphology of New England : u.s . Geological Survey Professional Paper, v. 1208 , 18 p. Erosion rates suggest that if the New England Highlands had not been uplifted in the Miocene, the area would now be largely a lowland . Lar.dscape is controlled primarily by bedrock . Glacial erosion and deposition during the Pleistocene have produced only minor changes .

Denny , C. S., and Goodlett, J. c., 1968 , Tree-throw origin of patterned ground on beaches of the ancien� Champlain Sea near Plattsburgh, N.Y. : u.s. Geological Survey Professional Paper, v. 600-B, p. B157-B164. Sorted circles only a few hundred years old form due to the formation and erosion of mounds and pits produ�� by the toppling of trees. Whatever patterns may have been on the surface of these benches during Champlain Se� time have been completely destroyed by the uprooting of trees.

Denny, c. s., and Lyford, w. H. , 1963, surficial geology and soils of the Elmira-williamsport region, New York-Pennsylvania: u.s. Geological Survey Professional Paper, v. 379 , 60 p. Authors discuss periglacial colluvium and the eff�ct of tree throw.

Des Marais, D. J. , 1981 , Subterra�ean stream pi racy in the Garrison Chapel karst valley, Indiana, U.S.A. , in Beck, B. F., ed., Eighth International Congress of Speleology Proce�ings: Huntsville, AL, NSS, p. 196-199 . caves in area reveal in detail the underground piracy of a southwara-draining surface stream by four westward-draining karst spring systems . The history of this drainage network has been revealed by dye tracing experiments and by studying cave-passage oorphology.

DeVitis, D. P. , 1974 , Relationship between selected morph�tric parameters and litho-structural controls in the Great Valley: A Cumberland Valley example [Ph.D. thesis]: Pittsburg, University of Pittsburg, 157 p. Author makes various c011100n oorphometric measurements of drainage ar.d topography and deoonstrates litho-structural control . Also provides detailed descriptions of regolith of all types.

Dickson, R. R. , 1959, Some climate-altitude relationships in the southern Appalachian Mountain region: American Meteorological Society Bulletin, v. 40 , p. 352-359 . Regression equations relating elevation to annual , January, and July mean temperatures and mean daily temperature ranges, to length of growing season, and to mean annual snowfall are derived .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Dietrich, R. V. , 1957, Mountain L,�e: 'tineral Industrh. Journal , v. 4, p. 7-8 . Author provides bri( f history of Mountain LaJ..e: and a sunmary of ideas on how it formed.

Dietrich, R. v. , 1957, Weathered stream gravels at the crest of the Blue Ridge [Abstract] : Virginia Academy of Sciences Proceedings for 1957, p. 330. Author reports deposit of alluvial cobbles and boulders near the eastern boundary of Floyd County, 5 miles S37W of the Roanoke-Montgomery-Floyd counties conmon point. Deposit occurs in the New River basin a few feet from the present Atlantic-Gulf divide , and shows that large streams once flowed here probably flowing to the west. If so , the Nett.· .ttiver basin must have once been much larger and must have included a sizeable area east of the present Blue Ridge escarpment .

Dietrich, R. v. , 1958 , Origin of the Blue Ridge escarpment directly southwest of Roanoke , Virginia: Virginia Academy of Science Journal , v. 9, p. 233-246 . Study area is located at the boundary between two distinct parts of the Blue Ridge province - the irregular mountain ridges drained by Atlantic streams and the dissected upland drained almost wholly by Gulf of Mexico streams. Evidence here s· .ggests that the location, as well as the character, of the present Blue Ridge escarpment is the result of migration of the asyn��etric Atlantic-Gulf divide . A general geomorphic history is suggested for the province for the time subsequent to the late Paleozoic establishment of New River.

Dietrich, R. V. , 1959, Geology and mineral resources of Floyd County of the Blue Ridge upland, southwestern Virginia: Virginia Polytechnic Institute Bulletin, v. 52 , 160 p.

Dietrich, R. v. , 1970, V • f(S •.• ) , in Holt, P. c. , ed., The distributional history of the biota of the southern Appalachians : V.P.I. Research Division Monograph 2: Blacksburg, VA, Vi rginia Polytechnic Institute , p. 67-99 . Most pertinent is the appPndix, "Inorganic �nvironments of the 'Appalachian Highlands' south of Pleistocene glaciation." Mainly physiography .

Oils, R. E. , 1957, A guide to the coweeta Hydrology Laboratory, Southeastern Forestry Experiment ::;tation, AsheYille, N.C. : Coweeta, NC, Coweeta Hydrologic Laboratory, 40 p. Author SUIII!Iarizes hydrologic and so:.l-erosion research at Coweeta . Effl!ct of logging, grazing on runoff and sediment yield discussed. Has isohyetal map for maximum wate.: year, forest cove r map.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Dinga , c. F. , 1971, An analysis ,2 the relationship between geologic structure and the geometric surface fonn of homoclinal ridges [Ph.D. thesis): Terre Haute , IN, Indiana State university, 219 p. Five mathematical models or hypotheses , based on a combination of the concepts of dynamUc �uilibrium, entropy, and denudation chronology, were formulated to explain the inverse relationship that exists between homoclinal ridge-crest height and structural dip in 3 regions (the V&R being one). No one hypothesis best fits the Valley and Ridge data. Either the models have failed to take into account certain important structural or lithological variables or the interpretation IIU.ISt be advanced that the ridges are in a state of disequilibrium, perhaps Otie to uplift, rapid topographic lowering due to limestone , or nearness to master streams .

Doehring , D. o. , and Vierbuchen , R. c. , 1971, cave development during a catastrophic stonn in the Great Valley of Virginia: Science , v. 174, p. 1327-1329. Observations before and after the catastrophic 1969 �lle stonns show that a substantial am:>unt of bedrock erosion can be accomplished in a cave during one flood.

Dole, R. B., and Stabler, H. , 1909, Denudation: U.S. GeOLvgical Survey Wa ter Supply Paper, v. 234, p. 78-93. Authors provide tables showing suspended-sediment loads of rivers, including some in the Appalchians .

Doughe rty, P. H., 1985, An ove rview of the geology and phys ical geography of Kentucky, in Dough ty, P. H. , ed. , caves and Karst: Kentucky Geol . Surv . Special Pub. 12, Series XI : Lexington, KY, Kentucky Geological Survey, p. 5-17. Mainly a physiographic description of the different regions of Kentucky .

Drahovzal , J. A. , 1968 , Phys iography of Alabama, in Copeland, C. W. , ed., Geology of the Alabama Coastal Plain - a guidebook: Alabama Geological Survey Circular 47: Alabama Geological Survey, p. 7-15. A brief description of the physiography of Alabama, by province .

Drake , M. E. , and Borden, J. D. , 1981, Complex groundwater basin migrations in Roppel cave , Kentucky, in Beck , B. F. , ed. , Eighth International Congress of Speleology Proceedings : Huntsville, AL, NSS , p. 28-30 . Roppel Cave consists of a series of large tubes and canyons that suggest a history of interbasinal groundwater pirades. Evidence consists of radical changes of flow directions that occur within the cave and scallops that indicate reversed flow directions . Authors provide a map.

Duckson, D. w. , Jr., 1981, Creeks, runs, and hollows : Professiona� Geographe r, v.33, p. 361-365. Demonstr;- �es that the popularly used tenns creek , run, and hollow do indeed connote stre&as of different size.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 'Xlncan , w. M. , Eddy , G. E. , Errington, P. R. , and .'lilliamson, D. B., 1968 , capture and diversion of runoff by subsurface channels : west Vi rgini� �cademy of Sciences, v. 39, p. 320-326 . In a region where limestone crops out along the eastern flank of Back Allegheny Mountain, it is found that sur�ace drainage is captured and diverted by underground stream channels. The subsurface flow parallels the ridge of the mountain, crosses unde r intervening ridges, and reappears as springs or resurgences one or more ravines to the north. The direction of the subsurface flow is controlled by the joints and their intersection with the dipping strata.

Dunford-Jackson, C. s., 1978 , The geomorphic evolution of the Rappahannock River basin (M.S. thesis] : Charlottesville, VA, university of Vi r�inia, 92 p. Recent detailea soil mapping provides an excellent data base for delineating the post-Miocene geomorphic history of the basin by means of correlation of fluvial terraces, examination of soil profileb on these terraces and quantitative recognition of relict features. A model is proposed for projecting subtle terrace deposits to a downstream plane , summing the occurrences at that plane , and determining possible gradients for previous stream levels on a quantitative basis. Correlation of the highest fluvial terraces in this study with the Brandywine &1d Pinehurst surfaces is suggested.

Dury, G. H., and Teller, J. T. , 1975, Paleogeamorphic and paleoclimatic implications of "preglacial" meanders in the Cincinnati area : Geology, v. 3, p. 5�5- 1586. A nor ..nward increase in meander waYel.ength of the Old Kent11cky River supports the earlier conclusion, based on 1ndependent evidence , that the river used to flow northward. The wavelength/drainage area rati�s for the abandoned meanders are different from those of existing stream meanders, a finding that indicates hydrologic conditions different from those of today .

Eargle, D. H. , 1940, The relations of soils and surface in the South Carolina Piedmont : Science , v. 91, p. 337-338. Hithe �:to, most Piedmont soils were thought to have developed from material of residual origin. The discovery of organic material underlying many soils, and evidence of migration within many soils (stone lines, clasts from upslope veins ), suggests many soils on the Piedmont are composed of transported material .

Eargle, D. H., 1946, Pleistocene soils of the Piedmont of south carolina (M.S. thesis]: Columbia, sc, university of South carolina , 60 ?· Author provides details oi colluvial soils described in his 1940 and 1977 articles.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Eargle, D. H., 1977 , Piedmont Pleistocene soils of the Spartanburg area, South carol ina: South Carolina Division of Geology Geologic Notes, v. 21, p. 57- 74. Mode rn soil profiles have developed in coll�ial and alluvial materials on the lower parts of hillslopes .�d in the valleys of small streams. The colluvilllll locally covers paleosols and Pleistocene organic deposits preserved beneath g[ound-water tables . Parent material of about 50 percent of Piedmont soils is transported material . The Pleistocene headwater landscape was more rugged than today's, being chatacterized by sharp divides and deep, steep-walled ravines and gullies etched in soft, friable saprolite. Modern slopes have developed in part by gully gravure.

Eaton, H. N. , 1919, Some suLordinate ridges of Pennsylvania: Journal of Geology, v. 27, p. 121-127. Author attempts to show that the "subordinate ridges" (i.e., those held up by rocks other than the Tuscarora) are more nume rous than previously supposed, that their origin and existence have not been explained satisfactorily, and that they threaten the validity of the Cretaceous peneplain theory.

Eckhoff, 0. B. , 1960, The hillslopes of the Piedmont of North Carolina [M.S. thesis): Chapel Hill, NC, University of North carolina , 77 p. Measured profi '1s show that nor��. northwest, and east-facing hillslopes are stee�r and have greater range or variation of the maximum angles than do the south, southwest, and west sides of hills. The main factor affecting valley asymmetry may have been erosion due to frost action on the sides and t0ps of hills, and consequent deposition near the bottom of hills. This action must have taken place during a colder climate.

Edmundson, R. s., 1940, Origin of Little North Mountain in Virginia: Journal of Geology, v. 48, p. 532-551 . Water and wind gaps generally occur at places whe re the Tuscarora sandstone is thin or absent, and the higher altitudes correspond to a thickening of this sandstone . TOpographic variation seem to have been largely controlled by sedimentation and to a less degree by the structure.

Eisenlohr, W. s., Jr., 1952, Floods of July 18, 1942, in north-central Pennsylvania: U.S. Geological Survey Water-Supply Paper, v. 1134-B, p. 59- 158. Description of the famous Johnstown flood. Mainly hydrology, but includes brief descriptions of:' debris flows, blow-outs, and slides.

Englund , K. J., and Roen, J. B., 1963, Origin of the Middlesboro basin, Kentucky: U.S. Geological Survey Professional ��r, v. 450-E, p. 20-22 . Authors suggest that the conspiculously different topography and the intense defotmation of rocks underlying the basin are due to an impact of a meteorite.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Epstein, J. B., 1966, Structural control of wind gaps ;-nd water gaps and of stream �apture in the Stroundsburg area, Pennsylvania and New Jersey: u.s. Geological Survey Professional Paper , v. 550-B, p. B80-B86. Wind and water gaps in study area are located where resistant rocks dip steeply and have a narrow width of outcrop , where folds die out over short distances, or where folding was more intense locally than nearby. Al l gaps trend about perpendicular to strike, and parallel to major cross-joint sets . These observations favor the hypothesis of structural r.ontrol of the location of stream gaps , rather than of regional supe rposition of the streams upon the resistant rocks.

Epstein, J. B. , and Epstein, A. G. , 1969, Geology of the Valley and Ridge province between Delaware wate r Gap and Lehigh Gap, Pennsylvania, in Subitsky, s., ed ., Geology of selected areas in New Jersey and eastern Pennsylvania: New Brunswic�. NJ , Rutgers University Press, p. 132-205. Authors briefly discuss structural co�trol of three gaps in Blue Mountain.

Epstein, J. B. , Sevon , W. D. , and Glaeser, J. D. , 1974, Geology and mineral resources of the Lehighton and Palmerton quadrangles, carbon and Northampton unti co es, Pennsylvania: Pennsylvania Topographic and Geologic Survey Atlas, v. 195c� , 460 p. Discuss shale-chip colluvium in some detail, �lder fields. Figure 121 is a cross-section through the south slope of Blue Mountain, showing colluvium thickness, which reaches 50-70 feet in many palces.

E-..• ensoh.l , F. R. , and Dever, G. R. , Jr., 1979 , Carboniferous geology from the Appalachian basin to the Illinois basin through eastern Ohio and Kentucky : Ninth International Congr�ss of Carboniferous Strat�graphy and Geology, Field Trip no . 4.: Lexington, University of Kentucky , p. 3-10. Shore section of book entitled "Physiography along the �i�ld-trip route" is pertinent .

EVenden, L. J. , J96�. Quantitati"e characteristics of dn- ' m.ge bc.sins in the

delimitation of ge0100rphic regions [M.A. thet . .LS ]: Athens,GI\, Univeristy of Georgia, 111 p. Analyzed morphometry of 23 drainage basins in 3 subp•ovinces of Piedmont Georgia and draws conclusions for states of developmenc. Used aerial photographs for morphometry.

Ewers, R. 0. , 1985, Patterns of cavern development along the CUmberland escarpment in southeastern Kentucky, in Dougherty, P. H., ed., r.aves and karst of Kentuc-ky : Ker •• Geol. Surv . Sp. Pub. 12, Ser . XI : Lexington, KY, Kentucky Geological Survey, p. 63-77 . Provides a theoretical model to explain t�e integration of the subsurface drainage system.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ewe rs, R. 0. , and Quinlan, J. F. , 1981 , Cwe rr. porosity develo[XUent in limestone : A low dip model from Mammoth Cave , Kentucky, in Beck , B. F. , ed .. Eighth International Congress of Speleology: Huntsville, AL, NSS , p. 71.7-731 . In IOOdel , a rectilinear tribt•,tary pattern of conduits evolves through a ste��ise integration of &�orter distributary elements wit� expanding w:dth and catchment area while the majority wi ll be of small extent close to the discharge bounda �. The levels of M.� th Cave which actively trans�i t groundwater appear to match the characteristics of the model .

Ewing, A. L. , 1885, An attempt to determine the amount and rate of chemical erosion taking place in the limestone (Calciferous to Trenton ) valley of Center County , Pennsylvania: American Journal of Science , v. 29 , p. 29-31 . An early effort to estimate the amount of chemical erosion in a limestone area . i'leasured grams of solid per liter , estimated flow velocity from surface floats . Estimated denudation rate at 34 nm/1000 yr .

Fadaie , K. , and Brown, L., 1984, Contemporary tilting in the central Atlantic Coastal Plain : Journal of Geology, v. 92 , p. 547-558 . Geodetic leveling across the Cape Hatteras arch between Norfolk , VA, and New Bern, NC , suggests an unusually large northward tilting. New Bern appears to have risen relative to Norfolk as much as 18 em between 1932 an:i 1963, and 26.6 em between 1963 and 1979 . These rates seem unrealistically large , not only with respect to the longer-term geologic estimates, but also in comparison with contemporary tide-gauge estimates of crustal movement. A detailed analysis of the leveling results was carried out to evaluate , to the extent possible , their validity as estimates of neotectonic movement. Results suggest systematic errors are possible.

Faye , R. E. , Carey, w. P. , Stamer, J. K. , and Kleckner, R. L. , 1980 , Erosion, gediment discharge , and channel morphology in the Uppe r Chattahoochee River basin, Georgia: U.S. Geological Survey Professional Paper, v. 1107, 85 p. Rat�s of sheet erosion were computed in 9 watersheds using

the Universal Soil Loss Equation ..•Erosio n yields were greatest in watersheds with the largest percentages of agriculture and transitional land uses . LOWest yields were in highly urbanized watersheds . Timber harvesting increased yields seve ral orders of JMgnitude .

fPr�eman , N. H. , 1936, Cyclic and non-cyclic aspects of erosion : Geological Society of America Bulletin, v. 47, p. 173-186 . Mentions Appalachians ; among other locations , in discussing cyclic and non-cyci'

Fenneman , N. M. , 1928, Physiographic divisions of the Uni ted States : Association of American Geographers Annals, �- 18, p. 261-353. on p. 292-309, delineates bounda ries of Appalachian Highland and Interior Low Plateau.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Fennaman, N. M. , 1938, Physiography of Eastern Un ited States : New York , McGraw Hili, 691 p. Book includes chapte rs on all provinces of the Appalachian Highlands and the Interior Low Plateau . GeomorpholO�i ur rc 19�Q is summarized.

�ennPman, N. M. , �� d Johnson, D. W. , 1930, �hysical divisions of the United States (map, scale 1:7,000,000]: Washington , DC, U.S. Geological Survey, 1 p. Map showing physiographic boundaries of the united StatPs.

Ferguson, H. r. , 1967 , Valley stress release in the Allegheny Pl�te3u: Association of Engineering Geologists L� •lletin, v. 4, p. 63-71 . Valleys show compression faults in b1e valley bottom and tension fractures in the valley walls. Thickness �asured in tens or hundreds of feet. Mylonite or gouge in the valley walls and Lottom �ndicate the bottom of the zcne of stress release . The horizontal movement produced by expansion, logather with the load, produce forces that cause a wedge failure of �� e valley walls and bottom in �� e form of arching, thrust faulting, or shear breaks in �� e rocks .

Fie��er, F. J. , 1967, Surficial geology of the Mountain Lake area, Giles County, virginia [M.S. thesis ]: Blacksburg, �. Viginia Polytechnic Institute , 108 p. Author finds evidence of at least two episodes of mass wasting in the Mountain Lake area, which he attributes to congeliturbation during glacial stages. Also contains good descriptions of physiography and geomorphology.

Fist. .-, r, c. c. I 1955 I Elongate mear.:iers of the North Fork of the Shenandoah River [�stract): Geological Society of America Bulletin, v. 66, p. 1687. Describes geometry and size of elongate incised meande rs.

Att ributes them to a single erosion cycl� •••says river has cut down � minimum of nearly 100 ft since it meandered broadly. says no elongated meanders are forming �oday.

F�- �L . s. P. , Far.aff, A. S., and Picking, L. w. , 1968, Landslides of Sl'Litheastern Ohio: Ohio Journal of Science , v. 68 , p. 65-80. Descrihes lithology and chemistry of cyclot�emic shales that are particularly subject to landsliding.

Fit.:patdck, M. �. , 1980, Origin of the present course of the Potomac River near Paw Paw , west Virginia [M.S. thesis): Terre Hau te, IN, Indiana State university, 73 p. Author provides evidence that a large meande r cutoff of the Potomac c-:curred when the Potomac wali captured by one of its tributi'lries, L�ttle Cacapon River, when lateral corrasion removed the civid� �tween the two streams .

Flacvus, E. , 1958, White Mountain landslides: Appala�hia, v. 32 , p. 17�-191 . Popular account of la�slides .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Fleming, R. w. , Johnson , A. M. , Hough , J. E. , Gokce , A. o. , and Lion, T. , 1S81, Engineering of the Cincinnati area, in Roberts, T. G. , ed ., GSA '81, Cincirutati - Field trip guidebook: Bould�r,CO, Geological Society of America, p. 543-570. Four of th� £1 �ld trip stops involve landslides and the fifth shows erosion-sedimentation problems caused by urbanization. Landslides in colluvium are included . Maps and cross sections of landslides are also included .

Flint, R. F. , 1963, Altitude , lithology, and the fall zone in Connecticut : Journal of Geology, v. 71 , p. 683-697 . The F&ll zone , a facet-like surface in coastal Connecticut , is identified with the sub-Cretaceous surface beneath Long Island. Probably it lay buried beneath a Cretaceous cover while the region north of it was deeply eroded . In place of the concept of superposition from a cover, it is more likely that the drainage pattern of the Fall Zone antedates that cover . The geometry of the Fall Zone implies recurrent (or continuous ) arching beginning before Late Cretaceous. Except for local deepening of major valleys, glacial erosion appears to have been minor, and little glacial rearrangement of drainage has occurred.

Foley, L., and Chapman, J. , 1977 , Stratigraphy and geomorphology of the Icehouse Bottom, Harrison Branch , and Patrick sites, in Chapman , J. , ed ., university of Tennessee Department of Anthropology Report of Investigations : Knoxville, Tennessee Valley Authority, p. 179-206 . Describes stratigraphy and geomorphology of floodplain and terraces at four sites along the Little Tennessee River.

Foose , R. M. , 1953, Ground-water behavior in the Hershey Valley, Pennsylvania : Geological Society of America Bulletin, v. 64 , p. 623-645. When a mine began pumping 6500 gpn frou1 lower levels in 1949, it drastically lowered the groundwater level ove r an area of 10 square miles, drying up most valley springs and many wel ls. About 100 sinkholes of all sizes developed in this area. Author systematically observed 100 wells and springs ; details of groundwater movement was studied with dye tracing.

Foose , R. M. , and Humphreville, J. A. , 1979, Engineering geological approaches to foundations in the karst terrain of the Hershey Val ley: Association of Engineering Geologists Bulletin, v. 16, p. 355-381 . Large numbers of catastrophic sinkholes developed in 1949 owing to extreme lowering of water table by pumping . Concerning construction, foundation conditions have revealed widespread karst conditions, characterized by pinnacle weathering and cavernous rock, undrained depressions and sinkholes .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Foss , J. E. , 1974 , Soils of the Thunde rbird site and their relationship to cultural occupation and chronology, in Garclner, w. M. , ed. , The Flint Run paleo-Indian complex : A preliminary report 1971-1973 seasons : washington, DC, Catholic university of America, p. 66-83. Figure 36 shows four major soil weathering zones: 1) levee and flood channel on the flood plain; 2) terrace and fan; 3) Clovis clay; 4) limestone residuum. Using radiocarbon date and archaeological dating, provides estjmated chronology of deposits and soils.

Foss, J. E. , Fanning, D. S. , Miller, F. P. , and Wa�1er, D. P. , 1978, Loess deposits of the Eastern s;.ore of Maryland: SoH Science Society of America Journal, v. 42, p. 329-334. Silt deposits appear to be loess. A radi ocarbon date indicates that they were deposited after 10,520 (plus or minus 240) yr B.P. Profile characteristics of soils developed in the loess show moderately well expressed argillic horizons .

Foss , J. E. , wagner, D. P., and Miller, F. P. , 1981, Soils of the Savannah Riv0r valley: Atlanta, �. National Park Service, 58 p. Published as Russell Papers 1985 by the National Park Service , Inter3gency Archeological Services, Atlanta , Georgia. Delineated 5 units, 4 of them alluvial . unit I soils are less than 250 yr old. unit IIa is 250-4,000 yr old, unit IIb is 4,000-6,000 yr, and unit IIC is 6,000-8,000 yr old. t� it III soils date between 8,000-10 ,300 B.P. unit IVa is 10,300-30, 000 and unit IVb is 100, 000-250,000 yr old. The upland residuum dates between 500,000 and 2,000, 000+ yr B.P.

Foster, S. S. D., Miwe , M. , and Price, M. , 1974, Hydraulics of sheetlike solution cavities: Discussion: Gra� Water, v. 12, p. 49. Authors cri.ticize G.K. Moore 's (1973) article for the mathematical methods used to estimate size of and nature of flow in solution cavi ties in central Tennessee.

Fox , P. P., 1941, Rate of s�lJtion of some limestone boulde rs in the Tennessee River: Tennessee Acade�r of Science Journal , v. 16, p. 333-335. Limestone riprap developed relief of one to three fourths inch between pure limestone and laminae of argillaceous or siliceous limestone ove r a period of 27 yr .

Fox , P. P., and West, T. M. , 1944 , Geologic profiles of the lower Tennessee River: Tennessee Academy of Science Journal, v. 19 , p. 150-159. Authors describe bedrock profile, alluvial profile, terraces, and dam excavations for the lower 60 mi les of the Tennessee River.

Franz , R. , and Slifer, D., 1971, Caves of Maryland : Maryland Geological Survey Educational Series, v. 3, 120 p. On p. 5-22, authors discuss geological setting and origin of l".a ryland caves.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 FraPzmeier, D. P. , Pedersen, E. J., Lo11gwell, T. J. , Byrne , J. C. , and Losche , c. K. , 1969, Properties of some soils in the CUmber!� Plateau as related to slope aspect and position: Soil Science Society of America Proceedings , v. 33, p. 755-761. Soils sampled on the lower, middle, and >�pper part ct steep north- and south-facing slopes in transects acrc ;s ridges. Particle size distribution, base saturation, and soil temperature are r'·later.l to slope position. Soils in middle slope are higher in coarse material than those in the upper or lower positions . Most eoils on the south-facir.g slL?eS have argillic horizons whi le most on north-facing slopes have cambic ones . Soils on N side have almost 2 degrees C la�r meanual ann temperature , more or�anic matter, a darker color, as well as holding more water during a period of \Yctter stress than soils on south-facing slopes .

Fridley, H. M. , 1929, Identification or erosion surfaces in south-central New York: Journal of Geology, v. 37, p. 113-134. Author says that region was peneplained and later uplifted and disser.ted. 'Ihis erosion surface is correlated •··:.':h the so-called Schooley peneplain in central Pennsylvania. Remnants of an older erosion surface, the Kittatinny, are demonstrated to exist on the highes� hills and ridges in southern New York �d in central and northern Pennyslvania . Erosion surfaces, younger than the Schooley and representing partial cycles of erosion, are r�cognized and traced by means : projected profiles along the Susquehanna River from Harrisbu.:g northward.

Fridley, H. M. , 1933, Drainage diversions of the Cheat River: West Virginia Academy of Science Proceedings , v. 6, p. 85-88 . Author hypothesizes that a pirate stream has eroded back through Chestnut Ridge , following, for ti." most part, the weak Mauch Chunk shales ana Greenbr.i�r limestone , and then has extended its drainage southward to a place whe re the capturing of the ancient Cheat River was effected.

Fridley, H. M. , 1939 , Solution and stream pi raLy: Journal of Geology, v. 47, p. 178-188. 'Ihe unusual course of the South Branch Potomac River through the famous Smoke Hole in eastern West Virginia is explained as stream piracy bmught about by underground solution of limestone .

Fridley, H. M. , 1940, Watergaps by solution and piracy - a reply: American Journal of Science , v. 238, p. 226-233. Author replies to Ve r Steeg's criticism of Fridley's 1940 paper.

Fridley, H. M. , 1950, 'Ihe ge0100rphic history of the New-Kanawha river system: We st Vi rginia Geological Survey Report of Investigations, v. 7, p. 1-12 . In •)ne section of the Teays between the sites of the present cities of Nitro and Huntington, We st Virginia, silt deposits were so deep that a new course of the river was established . The new course became a part of the present Kanawha River. The Pocatalico had carved a valley which in one place approached within about 2 miles of the Teays . 'Ihe diversion was accomplished simply by the erosion of a narrow divide composed of weak rock between the two valleys .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Fridley, H. M. , and Nolting, J. P. , Jr., 1931, Peneplains of the Appalachian Plateau: Journal of Geology, v. 39, p. 749-755. The ridges of the eastern part of the Appalachian Plateau of West Virginia and Pennsylvania show a marked accordance in elevation. Ridge tops are held up by resistant carboniferous sandstones. To the west of the ridges is a well defined erosion surface developed on much weaker upper carboniferous shales, sandstones, and limestones. A series of projected profiles of the topography , together with structure sections, reveals an accordance of hilltops and a beveling of strata which is convincing evidence of peneplanation. This surface is evidently much younger than that marked by the ridge tops farther east.

Fritz, S. J. , and Ragland, P. C. , 1980, Weathering rinds developed on plutonic igneous rocks in the North Carolina Piedmont : American Journal of Science , v. 280, p. 546-559 . Granites and adamellites develop few, but thick, clay-rich rindlets in the ir weathering-rind systems . Gabbro and syenites develop many, thin, limonite-rich rindlets concentric about cores of fresh rock. Orientation and propagation of solution channels in weathered rock control the appearar.ce of weathering rinds developed on that rock . However, these parameters are greatly influenced by dissolution-produced void space within the rock . Authors describe chemdcal processes involved.

Froelich, A. J., 1970, Landslide geology along south slope of Pine Mo��tain, Pineville to Harlan, in Geological Society of America Southeastern Section meeting guidebook, field trip 9: Boulder, co. Geological Society of America , p. 5-11. Stops include joint-controlled scarps in the lower Hance Formation, edge of ancient Tremont side , 01urch slide of 1968 , and structurally contorted shale-siltstone sequence .

Froelich, A. J., 1975.- Contour map of the base of saprolite, Montgomery County , Maryland [Map! ; ·1.S. Geological Survey Miscella.teous Investigation Se ries,

v. I-920-c , ' p.

Contour ..• ;terval is 50 ft.

Froelich, A. J., 1975, Surface materials map of Montgomery County, Maryland [Map]: u.s. Geological Survey Miscellaneous Investigations Series, v. I- 920-A, 1 F Map �-- _c, nclude artificial fill, alluvium, upland gravel deposits, Cod� .: Plain strata , saprolite (subdivided into that on one of 6 type� of crystalline rock ), and bedruck .

Froelich, A. ,J ., ;u,d Zennone , C., 1985, Maps showing geologic terrane , drainage basins, ove rh-pden, and low flow of streams in Fairfax County and vicinity,

Virginia: U . . Geological Survey Miscellaneous Series, v. I-1534, 1 p. overburde� is mapped as 0-10 ft, 10-50 ft, and greater than 50 ft. Rates relative �round-water storage and transmission capability in Piedmont and Triassic Lowland . Stief description of saprolite given. Figure 3 is diagrammatic cross section showing the relationship of ove rburden type and thic�ness to parent rock type and topography, to water table and drainage basin divides, and to urban development .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Frye , J. C. , 1940, Pleistocene diversion in the lower Muskingum valley region: Journal of Geomorphology, v. 3, p. 38-51 . Drainage changes were more complex than simple pending and resulting diversion across eels into adjacent valleys . In local areas the new drainage was developed with a large degree of disregard for the former drainage patterns. It seems probable that this development was controlled by backfilling, and progressive aggradation as outwash was carried into valleys further and further away from the ice front .

Gardner, J. V. , 1971 , A quantitative geomorphic study in the LeHigh River Delaware River section of the Great Va lley of Pennsylvania [M.S. the sis): Terre Haute , IN, Indiana State university, 81 p. Geometrical properties of 36 drainage basins developed entirely upon the Bushkill member of the Martinsburg Formation were measured . Used modal elevation determined from hypsometry as indication of erosion-surface level , as well as summit elevations . Results indicate there may exist remnants of two erosion su rfaces, one represented by the plane of accordant summits which slopes gently eastward toward the Atlantic, and the second by the plane of

accordant modal elevations •..

Gardner, L. R. , 1966 , The Pleistocene geology of the Brodheadsville and Pohopoco Mountain (7.5') quadrangles, Pennsylvania [M.S. thesis]: university Park , PA, Pennsylvania State university, 99 p. Mainly concerned with glacial geology, but good discussion of colluvium, particularly "shale chip gravel", which probably formed under periglacial conditions .

Gardner, L. R. , Kheoruenromne , I., and Chen, H. s. , 1981 , Geochemistry and mineralogy of an unusual diabase saprolite near Columbia, South Carolina : Clay and Clay Minerals, v. 29, p. 184-190. Discontinuities in the trends of Al203 , MgO, H20, and non extractable Fe203 apparently are related to redox conditions in the weathering profile because they occur at a depth where siderite veins first appear in the saprolite. These results indicate that where geochemical conditions favor retention of Fe ove r Al , smectites can form in preference to kaolinite or gibbsite even under conditions of strong leaching.

Garihan, A. B. L. , 1970, The influence of geologic and geomorphic parameters on the flood response of small drainage basins in Pennsylvania [M.S thesis): university Park , PA , Pennsylvania State university, 57 p. Author attempted to determine which geologic and geomorphic drainage basin parameters significantly affect the peak flood response for 19 drainage basins within 3 physiographic provinces. Not significant when considered singly were drainage basin shape , presence or absence of glaciation, mean a1mual precipitation, relief ratio, and amount of carbonate and coal . However, when the discharge coefficient, relief ratios, and drainage basin shape were tested together for association, the result was significant . The shale: sandstone ratio was found to be significantly related to the discharge coefficient in the Plateau but not in the Va lley and Ridge .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Gathright , T. M. , II, and Rader, E. K. , 1987, Recognition of disaggregated rock block slides in a structurally complex terrane in Virginia [Extended abstract): u.s. Geological Survey Circular , v. 1008, p. 34. Thirteen incised rock block slides , coherent to disaggregated , were identified on the dip slopes of East River and Peters Mountains and on the overturned beds of the Piney Ridge and associated hor£ � blocks. Lateral scarps, slip-off slopes, and sag ponds typical of rock block slides are poorly preserved on some of the slides. These disaggregated rock block slides have hummocky or ridged surfacee ranging in relief from 1 to 10 m. Some slides are sufficiently intact to preserve original stratigr�phic map uni ts . Several factors may contribute to the extensive disaggregation of these slides, including the proximity of thrust faults and the Giles County seismic zone , and the dissolution of carbonate rocks ove rridden by the slides .

George , A. I., 1976, Y� rst and cave distribution in north-central Kentucky : NSS Bulletin, v. 38, p. 93-98 . Author summarizes occurrence of karst features and caves in three counties of north-·central Kentucky.

George , A. I., 1995, Caves of Kentucky, in Dougherty, P. H., ed ., Cave� and karst of Kentucky: Ken. Geol . surv. Sp. Pub. 12, Ser. XI: Lexington, KY, Kentucky Geological Survey, p. 18-27 . Di scusses the distribution of caves in Kent-..:cky.

Gergel, T. J., 1964, Morphometric analysis of drainage basin characteristics on the Georgia Piedmont [M.A. thesis): Athens , C� , unive rsity of Georgia, 178 p. Author analyzed morphometry of fifth- and thi rd-order basins, and interprets the findings in terms of cyclic erosion and dynamic equilibrium.

Gersmehl , P. , 1973, Pseudo-timberline: The southern Appalachian grassy bald (summary) : Arctic and Alpine Research, v. 5, p. Al37-Al38. Downplays climatic and paleoclimatic factors in the existence of balds . Says that the ium:: nent disappearance of the grassy balds raises serious questions concerning their pre-European existence .

Geyer, A. R. , and Bolles, W. H. , 1979, Outstanding scenic geological features of Pennsylvania: Pennsylvania Topographic and Geologic Survey Envi ronmental Geology Report, v. 7, 508 p. Briefly descri�s 388 geological and geomorphological features in Pennsylvania, in popular te rms . A topographic map of each is provided.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Gibson, T. G. , 1970, Late Mesozoic-cenozoic tectonic aspects of the Atlantic Coastal margin: Geological Society of America Bulletin, v. 81 , p. 1813- 1822. Data from the middle and northern Atlantic Coastal Plain and continental slope show that the dominant filling of the Atlantic margin geosyncline occurred in pre-latest Cretaceous time with only thin additions of Cenozoic strata. Movement of detrital material into the offshore areas had largely ceased by latest Cret�ceou� t;mp, was essentially absent in the early Cenozoic, but increased consi1erably in the Miocene , indicating a rejuvenation of the Appalachian source area.

Gilluly, J., 1964 , Atlantic sediments , erosion rates, and the evolution of the continental shelf: Some speculations : Geological Society of America Bulletin, v. 75, p. 483-492 . Author estimates volume of Triassic and younger sediment on and offsnore from the Atlantic coast between Virginia and Nova Scotia, and compares this volume with that which would have been de rived from the probable source area at present rates of erosion. It is found that the ave rage rate of erosion in Triassic and later time was probably not less than three fourths of and perhaps equal to the present rate .

Gilluly, J., Reed , J. C., Jr., and cady , vl. M. , 1970, Sedimentary volumes and their significance : Geological Society of America Bulletin, v. 81, p. 353- 376. Authors estimate volume of Phane rozoic sediments off Atlantic coast (among other places) , then calculate an ostensible ave rage rate of Phanerozoic erosion of about l�.y., about one sixth of the present rate . Howeve r, present erosion is attacking a surface that exposes 76 percent sedimentary rocks, so that most of the current eroded sediment is of a recycled nature . The ostensible erosion rate is therefore spurious, and it is likely that the average erosion rate during the Phanerozoic was more than half that of present , and perhaps was nearly or quite equal to it.

Giwa , F. B., 1972, The relationship between structural dips and topographic dip slopes on the Allegheny Plateau [M.A. thesis): Pittsburg, University of Pittsburg, 76 p. Measured structl•.:al dips and dip-slopes and found a correlation of only 0.29 between the two . Measurement on 77 slopes was confined to the middle part of the slope . Mean dip was 4.8 and mean slope was 4.9 degrees, with the steepest about 12 degrees . Figure 10 (p. 72) is a scatter plot of slope angle against dip angle .

Glaser, J. D. , 1969, Petrology and origin of the Potomac and Magothy (Cretaceous ) sediments, middle Atlantic Coastal Plain: Maryland Geological Survey Report of Investigations, v. 11, 101 p. The Potomac Group and Magothy Formation (Early-Late Cretaceous ), the basal sediments of the Atlantic coastal Plain in Delaware, Marfland, and Virginia, were studied to determine the means of sediment dispersal , provenance , and character of the depositional environments . Mineralolgy and lithology indicate most sediment was derived from the Piedmont .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Glazzard, C. F. , 1981 , Streamflow characteristics related to channel geometry of selected streams on the Cumber- anj Plateau, Tennessee (M.S. thesis]: Knoxville, TN, University of Tennessee , 132 p. Attempted to estimate average andpeak discharges for 41 streams by means of channel geometry, to provide a tool for estimating these parameters on ungaged streams . Power-function equations were statistically developed using simple- and multiple-regression and structural analysis. For all equations , R-square values ranged from 0.834 to 0.926 .

Glenn, L. C., 1911, Denudation and erosion in the southern Appalachian region and the Monongahela basin: U.S. Geological Survey Professional Paper, v. 72, 137 p. A qualitative study of the effect of deforestation and consequent erosion of the steep mountain slopes on geologic, hydrolog�c, and economic conditions . From �J laski, VA, to Gadsden, AL. Provides detailed descriptions of slope erosion and effects on stream regilaent at many locations . Includes Ducktown, Tennessee . Has some nice photographs .

Godfrey, A. E. , 1975, Chemical and physical weathering in the South Mountain anticlinorium, Maryland: Maryland Geological Survey Information Circular, v. 19, 35 p. Author describes and maps periglacial features and other hillslope features. Suggests that unde r glacial climates, phy�ical weathering was domina ...... whereas today. chemical weathering is.

Godfrey, A. E. , Reesman, A. L. , and Cleaves, E. T. , 1971, The importance of chemical erosion: dynamic disequilibrium [Abstract] : Geological Society of America Programs ,.,i th Abstracts, v. 3, p. 767-768 . In limestone and serpentine rocks , chemical erosion greatly exceeds physical erosion, whereas the rates are more nP.arly equal in basins underlain by quartz, mica schist, and quartzite. The Catoctin-South Mountain area and the Central Basin of Tennessee are examples of disequilibrium in erosion rates in adjacent areas . By way of contrast, in the eastern Piedmont of Maryland, equilibrium ero�ion rates apparently exist between serpentinite , a rock that weathers primarily by chemi cal eros�on, and adjacent schist , a rock in which chemical and r.echanical erosion rates are subequal .

Goldthwait, R. P., 1940, Geology of the Presidential Range : New Hampshire Academy of Science Bulletin, v. 1, 43 p.

Goodlett, J. C. , 1954, Vegetation adjacent to the border of the Wisconsin drift in Potter County, Pennsylvania: Harvard Forest Bulletin, v. 25, 93 p. Diccu�sion of wind throw on p. 66-76 1s quite pertinent . Notes that disturbance of the upper parts of the surficial deposits by windthrow probably produces th e high degree of variability observed in soil profiles over short horizontal dista�ces.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Gottschalk, L. C., 1945, Effects of soil e•·osion on navigation in uppe r Chesapeake Bay : Geographical Review, v. 35, p. 219-238 . Provides cross sections showing progressive sedimentation at head of bay from 1846 to 1938 (Fig. 2). Figure 4 is a perspective sketch showing the original and present appearance of harbor at Port Tobacco. Figure 5 shows cross sections of sedimentation �f Patapsco River ann of Baltimore harbor between 1845 and 1924.

Grant, w. H. , 1962 , Weathering of Stone Mcuntain Granite : clays and Clay Minerals, v. 11, p. 65-73. weathering of the granite forms kaolinite, endellite, allophane , and gibbsite of which kaolin�te is the most stable. Bulk density ranges from 2.65 to 1.48 in saprolite, and is a good index of weathering. Biotite is the least stable original mineral, followed by oligoclase . Expansion of the rock in the early phases of weathering occurs but does not produce a significant increase in volume .

Grant , W. H. , 1964, Chemical weathering of biotite-plagioclase gneiss: Clay� and Clay Minerals, v. 12, p. 455-463. The weathering of biotite-plagioclase gneiss was studied unde r good drainage conditions in De Kalb County. A series of samples ranging from completely weathered to fresh rock werE' studied. The degree of weathering was detennined by bulk specific gravity and abrasion pH of samples in various rtages of decomposition.

Grant , w. H. , 1968, weathering, stceams, and structure in the central Piedmont of Georgia [Abstract ]: Georgia Academy of Science Bulletin, v. 26, p. 68 . In areas underlain by mica schists, the fold axes exert a strong control on stream directions, with valleys often 1 :curring on anticlinal structures. Streams were classified into those parallel to lineations, those parallel to joints, and those developed without obvious direction.

Grant , w. H. , 1983, Debris avalanching and slow alluviati0n, d mechanism for rapid valley gr�� [Abstract ): Geological Society of America Abstract� with Programs, v. 15, p. 55. Debris avalanches play a major role in mountain valley formation. They dam or otherwise impede stream flow, causing alluvial deposition behind the impediment. Result is rapid grown of mountain valleys composed of flat-bottomed valleys framed by steep mountains which are cut by v-shaped valleys .

Grantham, J. H. , and Velbel , M. A. , 1988, The influence of climate and topography on rock-fragment abundance in modern fluvial sands of the southern Blue Ridge Mountains, North Carolina: Journal of Sedimentary Petrology, v. 58, p. 219-227. Found that soils in watersheds with low relief ratios and high discharge per unit area experience the most extensive chemical weathering, and that sediments derived from these watersheds contain the lowest percentage of rock fragments.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Gtay, H. H. , Bassett, J. L. , Munson , C. A. , Munson , P. J., and Fraser, G. '5., 1983, Archaeological geolog�: of the Wyandotte Cave re

Gray, H. H. , and Powell, R. L. , 1965, Geomorpholo;y and groundwater hydrology of the Mitchell Plain and Crawford Upl&1d in southern Indiana: Indiana Geological Survey Field Conference Guidebook, v. 11, 26 p. A guidebvck and road log to the bedrock geclogy, su rficial geology, geoiiiOrphology, and hydrogeology of the Mitchell Plain and Crawford Upland , Indiana .

Gray, R. E. , Ferguson, H. F. , and Hamel , J. v. , 1979, Slope stability in the Appalachian Plateau, Pennsylvania and west Virginia, U.S.A., in Voight , F. , ed ., Developments in geotechnical engineering 14B, Rockslides and avalanches, part 2: New York, Elsevier, p. 447-471. Colluvial slopes tend to be 1.5-9 m thick on slcpes and generally increase in thickness (to maximum of 30 m) near :Jes of slopes . Movement surfaces may occur at several levels within the colluvial mass, but there is always a movement surface at the soil-rock interface . Movements have t:een reported on slopes as low as 10 degrees, and evidencg of pre-existing failure surfaces have been found on slope angles of 7-10 degrees .

Gray, R. E. , and Gardner, G. D. , 1977, Processes of colluvial slope develop;...::nt at McMechen, west Virginia: International Association of Engineering Geology Bulletin, v. 16, p. 29-32. TWo basic modes of colluvial soil accumulation on hillsides are identified: 1) on rock benches; and 2) in swales. The large colluvial masses, unless disturbed by construction activity, were assumed to be stable and to have de\'l'!loped under periglacial conditions . However , processes of �olluvial sl�pe development and a recent landslide, activated by abnormally high precipitation at McMechen, indicate that such colluvial masses form continuously and do not require periglacial coneitions .

Grender, G. c. , 1973, Slope distribution and relationship to bedrock in Appalachian Ridges near Roanoke, Virginia: American Journal of Science , v 273-A, p. 391-395 . Slope and bedrock lithology were compared at each of 2306 points in a 64-square-kilometer area. Points were 158 m apart. Slope distributions for 4 out of 5 gross lithologies were sufficiently distinct to suggest the possibility of using relative fequency tables of slope versus lithology as one criterion for gene:alized high-altitude mawing in limited terranes. Ve ry low slopes are strongly associated with Devonian shale. Very high slopes are strongly associated with sandstone .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Griffiths, J. c. , 1959, Size and shape of rock fragments in Tuscarora scree , Fishing Creek, Lamar, Cl inton 2ounty, central Pennsylvania: Journal of Sedimentary Petrology, v. 29, p. 391-401. Variation in size, sorting, and axial proportions of the scree is similar to variation in pebbles and quartz grains from other environments. No pattern of variation is evident over the small area studied.

Grim, R. E. , 1936, The Eocene sediments of Mississi�pi : Mississippi r� ological Survey Bulletin, v. 30, 240 p. Briefly considers implication of sediments for erosional history of Appalachians. Source area is determined to be southe rn Appalachians . '!his source area is believed to have been in the old age stage of physiographic development at the beginning of Eocene time . During Midway and Wilcox time it W'\S gradually uplifted so that by Wilcox time the youthful stage was reached. In Claiborne time that portion of this region remaining in the source area after the elimination of the Appalachian River had progressed to the stage of late youth or early maturity. By Jackson time it was again reduced to conditions of late maturity or old age .

GrootI J. J. I 1955, Sedift.>ntary petrolcgy of u.e Cretaceous sediments of northern Delaware in relation to paleogeographic problems : Delaware Geological Survey Bulletin, v. 5, 157 p. Chapter 7, "The Cretaceous development of the �palachian Mountain system in the light of the sedimentary record of the Coastal Plain" , is most pertinent. Attacks Johnson's theory of drainage superposition from a marine cover mass, for streams were eroding sediments from both Valley and Ridge and Piedmont during the Cretaceous. Up to the close of the Cretaceous , development of at most two peneplains can have taken place .

Groves, M. R. , 1976 , Preliminary report on groundwater resources of Rowan County, North Carolina: North Carolina Division of Environmental Management, Groundwater Section, Bulletin 22, 63 p. Contains maps and cross sections of saprolite thickness based on well logs.

Gryta, J. J., and Bartholomew, M. J. , 1983, Debri >-avalanche type features in Wautauga County, North Carolina , in Lewis, s. E. , ed., Geologic investigations in the Blue Ridge of northwestern North carolina: Carolina Geological Society Field Trip Guidebook: Raleigh, NC, N.C. Division of Land Resources , 22 p. In this area, debris-avalanche features are found in basins smaller in size and relief than those in central Virginia. Also, here the deposits commonly coalesce along bottoms of the valleys . Avalanches deposits es�cially plentiful in areas underlain by the mylonitic Cranberry Gneiss, probably because o£ �xtensive saprolite. Toe incision probably �ccurs soon af�er and possibly during the wa lng stages o£ the debris-avalanche episode .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Gryta, J. J. , &ld Bartholomew, �. J. , 1987, Frequency and susceptibility of debris avalanching induced by �J rricane Camille in central Virginia [Extended abstract ]: u.s. Geological Surve7 Ci rcular, v. 1008, p. 16-18 . Three susceptibility classes were defined on the basis of debris avalanche frequency: 0-Z , 2-7 , and greater than 7 avalanches per square km. Data suggest that 5 of the 12 bedrock units in the area are particularly susceptible to debris avalanching. The Crossnore Conq:>lex plutonic rocks are highly susceptible . Avalanches vrere most conm:m on NE- ,E- ,SE-, and NW-facing slopes.

Gupta , A. , and Fox , H. , 1974, Effects of high-magni tude flcods on channel fon.. : A case study in Maryland Piedmont : Water Resources Research, v. 10, p. 499-509. Among the more striking �ffects of the storms were destruction of floodplain vegetation, widening of stre&n channels, and clearing of the channels of all but very coarse materials. Low &ld medium flows succe�ding each �lood reduced enlarged channel widths by building up bar remnants with fines and fcrming new bars along channel margins, tending to destroy the evidence of such floods. Channels rreserve flcod-origin?ted forms Nhen high-magnitude floods occur with suffic;ent .egularity.

Hack , J. T. , 1955 , Geo!�r of the Brandywine area and orig! n of the upland of

southern Maryland: U. :'. Geological Survey Professional Pa�;>er, v. 2E7-A , 43 p. Inve�;tigates origin of upland deposits. ConcJudes that no Pleistc-cer.e marine transgressior1s have occurred at altitudes above 100 feet at a date later than ti1e deposition of the upland deposits .

Hack , J. T., 1957, Studies of longitudinal stream pro�iles in Virginia and Maryland: u.s. Geological Survey Professional Paper, v. 294-B, p. 45-97 . Investigated control of drainage area, size of bed material ,

and lithology on stream gradients . Derived equation: S • 18 (��) to the 0.6 po·wer.

Hack , J. T., 1960, Interpretation of erosional topography in humid temperate regions : Americar1 Journal of Science , v. 258-A , r. 80-97 . Hack's seminal paper on rlynamic equiHbrium. According to this concept , eve ry slope and every char1nel in ar1 erosional system is adjusted to every other. When the topography is in eqtilibr·umar1d erosional energy remains the same , all elements of the topog aphy are downwasting at the same rate. Large areas of erosionally graded topography in h�d regions have been considered to be "maturely dissected peneplains ." According to thE' equilibrium theory, this topography is what we should expect as the result of long continued eros�Jn.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hack , J. T. , 1960, Relation of solution features to chemical chacacter of water in the Shenandoah Valley, Virginia ; u.s. Geological Survey Professional Paper, v. 400-B, p. 387-390. Briefly discusses differences in chemistr'l of wat-:!r i11 4 streams typical of the Shenandoah Valley and relation to occurrence of sinks. Notes that sinks are abundant in carbonate rock areas flanked by highlands of clastic rocks from which waters of low alkalinity issue . Sinks tend to be further J ocalized alcag streams that drain clastic rocks. Solution features alsv appear to be especially nume rous in areas where the -��ks have low dips .

Hack , J. T. , 19�5, Geomorphology of the Shenandoah Va lley, Virginia and We st Virginia, and origin of the residual ore deposits: u.s. Geological Survey Professional Paper, v. 484, 83 p. Applies dynamic equilibrium concept to landscape evolution. Because of the steeper slopes required to transport the resistant rocks, streams in regions of resistant rock have a greater fall than those in soft-rock areas, a fact that accounts for the mountainous topography . The local relief in any given kind of rock is the same . In mountain areas, thick residuum is found only on rocks that contain components s•1bject to differential chemical and mechanical weathering. The ess0ntial requirement for the formation of an area of alluvium is a pronouncPd difference in the resistance of the bedrock in different parts of a drainage basin. Also discusses terraces, solution features, physiographic history.

Hack , J. T. , 1966 , Circular patterns and exfol iation in crystalline terrane , Grandfather Mountain area , N0rth Carolina: Geological Society of America Bulletin, v. 77, p. 975- J86. Aerial photos reveal nume rous large-sc< le, arcuate , circular, and elliptical patterns with diameters from 1000 to more than 4000 feet. They are c0111110nly defined by curving streams, curving ridges, and curving belts of contrasting vegetation . Geologic �vidence indicates that they are related to exfoliation or 3heeting.Rock spalls up to half a mile in diameter may be formed by dilation of the rock as the erosion surface is lowered . The spalls enable tectonic joints to open, forming thin layers of rock of differing permeability and susceptibility to erosion.

Hack , J. T. , 19�6, Interpretations of the CUmberland Escarpment and Highland Rim, south-central Tennessee and northeast Alabama : u . ... Geological survey Professional Paper, v. 524-c, 16 p. Attacks previous interpretation of the topography as the product of periods of base leveling, applies equilibrium concept . Suggests landscape could have formed by continuous lowering of the surface , a process that involves slope retreat on beds of different resistance. This interpretation is supported by the distribution and characte . of the surficial deposits , wh ich are adjusted to the outcrop pattern of the rocks now exposed.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hack , J. '1 ., 1969 , The area, its geologf ·.nozoir develc{XIlent of the southern Appalachians , in Holt , P. C., ed ., d�str: butional hi story of the biota

of the southern Appalachians, Part ,lVei . ;;;Jrates : Blacksburg, VA, Virginia Polytechnic Institute, p. }. Hack provides brief introduction to Appalachian geomorphology, then attempts to convince biologists t..h at .:;tream divides do not move around as much as they like to im�1ine. Notes that simple geometric principles show that di . 1de migration over great distances can be accompl ished only th rvugh very long periods of geologic time.

Hack , J. T. , 1973, Drainage adjustment in the AppaJ.achians , in Morisawa , M. , ed ., Fluvial geo1110rphology: Binghamton Sympos-ium in Geo1110rphology no . 4, London, Boston, Allen & unwin, p. 51-69 . Di scusses adjustment of major Appalachian streams to major lithologic distribution by means of a study of longitudinal stream profiles. A contour map on large streams shows that the general height of lruld is just west of the Atlant ic-Mississippi drainage divide . Se!ected stream profiles are analyzed by Hack's gradient index. This suggests that the position of the highl�nds is determined by a partial adjustment of the profiles of the major streams to the regional rock pattern . Some areas in the Appalachians are not in adjustment , however.

Hack , J. T., 1973, Stream-prof.:.le analysis and stream-gradient ind• x •.lournal of u.s. r search of the Geological Survey, v. 1, p. 421-429 . Discusses gradient-index concept , which allows meaningful comparisons of channel slope on streams of di fferent sizes, and applies it to streams i� several Appalachian provinces. Basically the index is the product of the channel slope at a point and the channel length measured along the longest stream above the point where the calculation is made . Demonstrates relation to lithologic variation.

Hack , J. T. , 1976, Dynamdc equi librium and landscape evolution, in Melhorn, w. N. , and Flemal , R. C. , eds. , Theories of landform developnent : Binghamton Geomorphology Symposium no. 6: Binghamton , NY, S.U.N.Y. Binghamton , p. 87- 102. Applies dynamic equilibrium concept to landscape evolution IIIOde.l.s that assume 1) a stable base level; 2) a rise in base level; and 3) a fall in base level. Uses examples from Appalachians . Mentions floor of the Shenandoah Valley, stream gradient-index , accordance of suromd ts in Valley and Ridge .

Hack , J. T. , 1980, Rock control and tectonism - their importance in shaping the Appalachian Highlands : u.s. Geological Survey Professional Paper , v. 1126- B, 17 p. Topographic analysis indicates that 1110st of the Appalachian landforms owe t..h ei r origin to erosion of rocks of different resistance rather than to tectonic processes. Cites some areas, however, where differences in relief are unaccounted for by geology (e.g., the Blue Ridge escarpment ), and thus may imply differential Cenozoic uplift . Tables 2 ard 3 show various estimates of erosion rates and tilt rates, respectively.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hack , J. T. , 1982, Physiographic divisions and different1al upl ift in the Piedmont and Blue Ridge : u.s. Geological Survey Professional Paper, v. 1265, 49 p. Divides Piedmont and Blue Ridge into six subregions that have somewhat diffe: �nt geologic3l histories during the Cenozoic Era : Piedmont Lowl�•ds , Not theastern Highlands , Southwestern Highlands , Foothill zone , Northern Blue Ridge, and Southern Blue Ridge . Discusses geomorphic evidence of differential upli �t, evolution of Blue Ridge escarpment, and time frame of late Teet nism.

Hack . J. T., 1989, Geomorphology of Lq e Appalachian Highlands , in Hatcher, R. D. , Jr. , Thomas, w. A. , and Viele, G. w. , eds., The geology of North America: The Appalachian and Ouachita regions : u.s. : Boulde r, CO, Geological society of America, in press. A general de scription of physiography of the Appalachiru1s, by province . Includes major features of s�rficial geology and morphological effects of glaciation.

Hack, J. T •. and Durloo, L. H. , Jr., 1962 , Geolngy of Luray Caverns : Virginia Division of Mineral Resources Report of Ir.vest1gatior· , v. 3, 43 p. A general discussion of cave featurf,s and possiblt:: origin, complete with maps and cross sections .

Hack , J. T. , and Goodlett, J. C., 1960. Gcv�rphology and forest ecology of a oountain region in the central Appalachians : u.s. Geological Survey Professional Paper, v. 347, 66 p. Authors define hollow, nose , and sideslope , and relate nature of the surficial mantle and fore&t type to the topographic setting. A special study was made of asyometric landforms . Also describe the effects of a catastrophic flood on hillslopes and floodplains .

Hack , J. T., and Newell, w. L. , 1974, North Carolina glaciers: Evidence disputed : Science , v. 184 , p. 88-91 . Authors dispute Berkland and Raymond 's (1973) claim of glaciation on Grandfather Mountain.

Hack, J. ·r ., and Young , R. s. , 1959, Intrenched meande rs of the North Fork of the Shenandoah River, Virginia: U.S. Geological Survey Professional Paper, v. 354-A, p. 1-10. Authors conclude that the meanders are caused by strong planar and prismatic structures in the Martinsburg shale that favor NW-SE differential erosion. There is no reason to believe that the river has been intrenched from an erosion surface on which the relief was less than that of the present upland or that changes in base !eve! have ir.fluenced the meander development .

Hadley, J. B., and Goldsmith, R. , 1963, Geology of the eastern Great Smoky Mountains , North Carolina and Tennessee : u.s. Geological Survey Professional Paper, v. 349-B, p. B1-B118. Plate 2, geology of the Dellwood quadrangle, includes surficial deposits: fans (2 ages shown ) and terraces (2 ages shown) . SurficiBl deposits are discussed on p. 107-111. Authors suggest that fan� were deposited in mid and late Wisconsin unde r glacial conditions .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hall, R. D. , 1976, Investigations of sinkhole stratigraphy and hydrogeology, south-central Indiana : NSS Bul letin, v. 38, p. 88-93. For content , see Hall's 1976 article in Geology .

Hall, R. D. , 1976 , Stratigraphy and origin of surficial deposits in sinkholes in south-central Indiana : Geology, v. 4, p. 507-509. ThP. nature and distribution of lithostratigraphic units suggest the filling of bedrock basins. The terra rossa in the sinkholes is primarily a transported sedimentary deposit. Th" source of much of the terra rossa sediment is probably the adjacent uplands .

Hamel , J. V. , 1980, Geology and slope stability in western Pennsylvania: l�sociation of Engineerir.g Geologists Bulletin, v. 17, p. 1-26 . Discusses shear zones and failure surfaces in colluvial slopes and provides geotechnical data . Several cross-sections of landslides are presented diagrammatically.

Hamilton, D. K. , 1948, Some solutional features of the limestone near Lexington, Kentucky: Economic Geology, v. 43, p. 39-52 . Solution has been effective only to a limited depth below the land surface . The bottom of the solutional zone is an exag')erated replica of the land surface , showing a greater depth of the solutional zone below stream valleys . The greater depth is attributed to the greater accumulation of ground water in those areas. Modifications of the ideal condition are effected by the less soluble beds and the configuration of the land surface. The underground drainage systems of the area develop in a manner similar to rectil inear stream patterns, showing a definite alignment along the two joint sets of the area. Contains some useful hypothetical cross sections.

Hamilton, D. K. , 1950, Areas and principles of groundwater occurrence in the Inner Bluegrass Region, Kentucky: Kentucky Geological survey Bulletin (Series 9), v. 5, 68 p. On p. 23-39 are discussed solutional features, similar to auth0r' s 1948 article .

Hamilton, W. , 1961, Geology of the Richardson Cove and Jones Cove quadrangles, Tennessee : u.s. Geological survey Professional Paper, v. 349-A , 55 p. On p. A47-ASO, author briefly discusses surficial deposits of the Smoky Mountains. Says fans merge too complexly to be easily classified. Only surficial deposit on map is alluvium.

Hanley, J. T. , 1976, Structural geomorphology of the Catawba Mountain Knolls, Roanoke r.ounty, Vi rginia [M.S . thesis): Syracuse , NY, Syracuse university, 85 p. Obsequent streams have dissected the secondary ridge and created regularly spaced conical hills, 65-175 m highe r than the adjacen� valley floor. There appears to be a striking regularity of spacing. Joints in the Bays Formation enhance the obsequent stream paths. A one-dimensional Fourier analysis isolated 4 essential frequency packets that define the topographic profile of the knolls, with cycle spacing of 590, 944, 1416, and 1890 ft.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hanley, J. T. , 1977, Fourier analysis of th·� Catawba Mountain knolls, Roanoke County, Virginia : Mathematical Geology, v. 9, p. 159-163. Similar to thesis. Distribution of spaci�g is not significantly differen� from a normal distribution having a mean of 240 m and a standard deviation of 60 m. Figure 1 is topographic map of the knolls.

Hanna , w. E. , Daugherty, L. A. , and Arnold, R. w. , 1975, Soil-geomorphic relationships in a first-order valley in central New York: Soil Science Society of America Proceedings , v. 39, p. 716-722 . Initial drift deposits �-ere modified by solifluction and then altered by fluvial aggradation-degradation under a periglacial environment , and by erosion in more recent times. Eight soil profiles representative of the geomorphic components forming the watershed were evaluated .

Happ, S. C. , 1934, Drainage hi story of southeastern Ohio and adjacent West Virginia: Journal of Geology, v. 42, p. 264-284. Topographic maps strongly support Tight's restoration of former main drainage lines in this area, but suggest numerous cl1i•• 1ges of detail, and the possibility of a more complex history than Tight recognized . Structural control is abundantly indicated , and may have been a factor in some of the drainage changes . Indirect evidence , of uncertain validity, suggests that at least part of the present drainage may have been superposed from a sedimentary cover more continuous than the valley silts, which Tight considered th� cause of the drair�ge changes.

Happ , S. C. , 1938, Geomorphic history of the Minisir� Valley region: Journal of Geomorphology, v. 1, p. 199-223. Discusses possible erosion cycles and drainage evolution in the area.

Happ, S. C., 1945, Sedimentation in South Carolina Piedmont valleys : American Journal of Science, v. 243, p. 113-126 . Valleys are aggraded by deposition of sand and reddish, micaceous , sandy silt, which are believed to be the products of soil erosion during the agricultural period of about 150 yr . '!he "modern" deposits cover a dark topsoil horizon, believed to represent the more stable alluvial surface prior to �o.hite settlement and clearin1 of the forests . 'Ihe ave rage thickness of "modern" deposits is about 4 ft, which is equivalent to removal of about 3.1 inches from the tributary uplands . Eros.on surveys by scs methods indicate about twice this amount of soil loss .

Harmon, R. S., 1979, An isotopic study of groundwater seepage in the central Kentucky karst: water Pesources Research, v. 15, p. 476-480. Author measured 018/016 ratios in precipitation and in vadose seepage at Great Onyx cave . Results show that short-term fluctuations in the 018/016 ratio of seepage wa ter in the vadose zone above the cave do not affect the oxygen isotopic composition of the speleothem calcite precipitated in the cave .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Harmon, R. s. , 1981 , Paleoclioatic information from isotopic studies of speleothems : A review, in Mahaney, w. c. , ed. , Quaternary paleoclimate : Norwich, England, Geo Books, p. 299-318. Discusses five types of information on Pleistocene climati2 change that canbe provided by natural variations in the isotopic composition of speleothems . Includes some examples from Appalachians.

Harmon, R. S., Schwarcz , H. P. , and Ford, D. c. , 1978 , Stable isotope geochemi stry of speleothems and cave waters from the Flint Ridge-Mammoth cave system, Kentucky : Implications for terrestrial climate change during the period 230, 000 to 100,000 years B.P. : Journal of Geology, v. 86 , p. 373-384. 0, H, D, U, and Th isotopic variations measured. Ages were determined by the Th230/U234 method. 018/016 ratios indicate that the maximum interglacial/glacial temperature decrease at thi s site was about 12 degrees c. wa rm conditions indicated at about 215,000, 195,000, 185,000-165,000, 125,000, and 105,000 yr B.P. Major cold periods are observed from 215,000-195,000 and 160,000-130,000 yr B.P,

Harmon, R. S. , Thompson , P., Schwarcz , H. P. , and r�rd, D. c. , 1976 , Dating of speleothems related to the ge01110roh.; c history of carbonate terrains , in Panos , V. , ed ., Sixth International Congress of Speleology Proceedings : p. 133-139. Briefly discusses centra! Kentucky karst, among other places. 'lWo stalagmites from the Davis Hall and Great Onyx areas of Malllooth cave , both of them upper levels, have been analyzed. The dates are out of the range of the Th230/U234 method (greater than 350, 000 yr old), and thus indicate that the upper levels of tne Mallmoth cave-Flint Ridge cavern system are at least "pre-Kansan" in 'Je.

Harmon, R. s. , Thompson, P. , Schwarcz, H. P., and Ford, D. c. , 1978, Late Pleistocene paleoclimates of North America as inferred from stable isotope studies of speleothems : Quaterrury Research, v. 9, p. 54-70. Includes caves from Kentucky and west Virginia, among others. 018/016 ratio curves for the sites show the following synchronous climatic fluctuations : warm periods from 190 to 165 and from 120 to 100 Ka, at 60 and 10 Ka, and cold periods from 95 to 65 and from 55 to 20 Ka. The periods of thermal maxima correspond in time to the interglacial periods of the marine foraminiferal isostopic and faunal temperature records and to periods of high sea stand as observed from radiometric dating of raised coral reefs.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Harrington, c. D. , and Tew, r.. H. , 1979, A geomorphic analysis of the pre Cretaceous erosion surface beneath the inner Coastal Plain of Harnett and Cumberland counties, North Carolina [Abstract]: Geological Society of America Abstracts with Programs, v. 11, p. 181. n1e geomorphic character of the buried surface on crystalline rocks was exandned using geologic data from wat�r wells in Harnett and Cumberland Counti�s, North carolina . Cc::-.puter-drawn contour maps and perspective views generated from the data show buried valleys whose sizes and courses generally coincide with those of present surficial drainage . Trend surface analysis of the data permits tre recognition of major pre-cretaceous streams as curvilinear anomalies lying below the first-order surface .

Harris, L. D. , 1973, Areas with abundant sinkholes inKnox County, Tennessee : U.S. Geological Survey Folio [Map] , v. I-767-F, 1 p. Map of scale 1:125,000 showing areas with abundant sinkholes , plus all limestone areas. Brief discussion and some small hypothetical cross sections.

Harris, L. D. , 1973, Basins drained by sinkholes in Knox County, Te�essee: u. s. Geological Survey Folio [Map), v. I-767-G, 1 p. Map shows drainage basins that drain to sinkholes , also area of Ten Mile Creek draina;c oasin that could be flooded if the sinkhole outlet of Ten Mile Creek were plugged .

Harris, w. G. , Iyengar, S. s. , Zelazny, L. w. , Parker, J. C., Lietzke , D. A. , and Edmonds , w. J. , 1980, Mineralogy of a chronosequence formed in New River alluvium: Soil Science Society of America Journal, v. 44, p. 862- 868 . The mineralogy of four soils (TO, T1 , T2 , T3 ), formed in progressively older New River alluvi'l.Dll, was studied with the assumption that trends could be attributed to age differences. Predominance of quartz and resistant heavy minerals in T2 and T3 suggests a wide time gap between T1 and T2 . Numerous aspects of weathering were exandned.

Haselton, G. M. , 1973, Fossible relict glacial features in the Black Balsam Knob and Richland Balsam area, North Carolina : Southeastern Geology, v. 15, p. 119-125. Small ice masses may have developed in the upper portions of the ravines above 4800 ft (1218 m). Striated quartz veins have been found at two locations, but may be result of faulting. The upper reaches of the largest ravines that face east, southeast, and north have cirque-like forms that have been modified by mass-wasting processes. Abundant boulder talus and block streams demonstrate a cooler former climate and suggest that treeline was lower.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Haselton , G. M. , 1974, Some reconnaissance geomorphological observations in northwestern South Carolina and adjacent North Carolina: South Carolina State Development Board, Division of Geology, Geologic Notes, v. 18, p. 60-74. Map (Fig. 1) shows location of high gravels. Highest stream terraces occur 100 ft above the Saluda River. Foliation and jointing control stream direction - rose diagram of joints included . An erosion surface between 28JO and 3200 ft is described, plus other less-well developed surfaces. The Blue Ridge scarp is also briefly discussed.

Haselton, G. M. , 1979, Further observations on glaciation in the Black Balsam Knob and Richland Balsam area, North Carolina , in Raymond , L. A. , ed. , Second Annual Confecence on the Quaternary History of the southeastern United States Proceedings : Boone , NC , Appalachian State University, p. 6- 10. Discusses evidence for absence of glaciation in the southern Appalachians.

Haselton, G. M. , 1979, Further observations on glaciation in the Shinir_:�ock area, North Carolina : Southeastern Geology, v. 20, p. 119-127. Discusses geomorphic evidence that Pleistocene glaciation in the Shining Rock Quadrangle is very unlikely.

Hatch, L. , 1917, Marine terraces in southeastern Connecticut: American Journal of Science , v. 49, p. 319-330. Projected profiles show excellently the character of the upland as a succession of terraces facing the sea and stepping down from 500 ft through 400, 300 , 200, and 100 ft . Attributes these terraces to wave action.

Hayes, C. W. , 1895, The southern Appalachians : National Geographic Monograph , v. 1, p. 305-336. Discusses physiographic divisions, description of the physiographic divisions, drainage, physiographic development , relation of recent upl ift and present uplift, and the influence of physiography on social and industrial development .

Hayes, c. w. , 1899, Physiography of the Chattanooga district: U.S. Geological Survey Annual Report, v. 19, p. 1-58. Plates 2 and 3 are maps owingsh development and preservation of peneplains in the district. Figure 1 is a curve illustrating the relation of topographic relief to lithologic compositi��- Notes that it is entirely conceivable that the drainage oi the Appalachian Valley may again be diverted southward to the Qllf, for the Coosa has a decided advantage ove r the Tennessee in its :ncre direct course to the sea . on p. 24 discusses correlation of peneplains.

Hayes, c. W. , and Campbell, M. R. , 1900, The relation of biology to physiography: Science , v. 12 , p. 131-133. Au' ·ors invoke Simpson's assumption that the di stributicn of mcllusc �pecies support former drainage of the Tennessee River to the coast via the present Coosa and Alabama Rivers, to bolster their own theory of this event based upon physiographic evidence .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hayman, J. W. , 1972, The significance of some geologic factors in the karst development of the Mt . Tabor area, Montgomery County, Virginia [M.S. thesis) : Blacksburg, VA, Virginia Polytechnic Institute, 46 p. The intensity of karstification as measured by sinkhole density was studied. In dolomite terrane , a statistically significant correlation exists between increasing sinkhole density and increasing Ca;Mg ratio of the rock . Sinkholes are pr�valent in some limestone or dolomite units but absent in others. Rea5on probably related to internal fabric of the rock . Sinkholes are generally elongated in the direction of a prominent joint set .

Haynes, C. V. , 1985, Mastodon-bearing springs and late Quaternary geochronology of the lower Pomme de Te rre Valley, Missouri : Geological Soc�ety of America Special Paper, v. 204, 35 p. A radiocarbon-dated (154 dates) chronostratigraphic sequence 1n four terracP.s reflecting five major episodes of aggradation and degradation is described. Probably all of Wisconsin time and the Holocene is represented. A sixth alluvial deposit is probably Illinoian and possibly even older. Spring deposits within the terraces contain bone beds associated with peat lenses containing pollen, plant, and beetle remains. Springs appear to have erupted initially near the peak of a glacial maximum. A major episode of degradation occurring between 10,500 and 13,000 yr BP probably coincides with similar episodes occurring about 12,000 yr BP on many streams in the u.s.

Haynes, C. W. , and campbell, M. R. , 1894, GeOIOOrphology of the southern Appalachians : National Geographic Magazine, v. 6, p. 63-126 . Plates show deformed Cretaceous and Tertiary peneplains. Discuss physiographic development, drainage evolution, diversion of the Appalachian River.

Hedges, J., 1975, Multiple cy�les of cryoplanation on Sugarloaf Mountain, Maryland: Biuletyn PP.ry:1lacjalny, v. 24, p. 233-244. Periglacial feutuces on this mountain of elevation 1280 ft include tors, shattered ledges, taluses, block streams, cryoplanation terraces. Two perigl acial episodes, probably Illinoian (tor and suami.t plateau) and �Jis,.onsin (!.�ge , talus, terrace , and block stream) in age , are represe��ed .

Heinecke , T. A. , 1982 , Magnetostratigraphic correlation between terraces of �� Green River and sediments within the passages of Malllooth cave National Park, Kentucky [M.S. thesis) : Pittsburg, University of Pittsburg, 67 p. Magnetostratigraphic correlation of Green River terrace sediments to sediments at corresponding elevations in the passages of Malllooth cave suggests that both types of sediments were deposited contemporaneously and recorded the same magnetic polarity. Portions of the terrace sediment&, however, appear to have been subjected to bioturbation or oxidation, whic� has resulted in the destruction of their original magnetization.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Heller, S. A. , 1985, Karst topography of central Greenbrier County , West Vi rginia: Southeastern Geology, v. 26, p. 111-116 . Examines the surface karst features in relation to the structural , stratigraphi c, and hydrologic setting. Geologic structure controls the pattern of many surface and subsurface streams in the area. Differential erosion among the limestone units within the Greenbrier Group determines whether the land surface is a smooth plateau or steep and karren-covered.

Helvey, J. D., Hewlett, J. D. , and Doug.iass, J. E., 1972, Predictinc;. <: , moisture in the southern Appalachians : Soil Science Society of A. r Proceedings, v. 36, p. 954-959. Soil moisture was measured for 3.5 yr on forested slopes near Coweeta Lab in order to develop equations for predicting soil moisture content of watersheds . Predictors used were precipitation and easily measured topographic, seasonal, and soil physical factors; among these, sand content and moisture retention at 1-bar suction were the best predictors . Position on slope appsared to be an important factor only in the lower 25% of the slope . Equations developed account for about 88% of the •1a riation in soil moisture .

Hempel , J. C., 1974, A preliminary study of the effects of lithology on cave entrance locations within the Union Limestone Formation of the Greenbrier Group, Monroe County, We st Virginia, in Rauch, H. w. , and werner, E., eds. , Fourth conference on karst geology and hydrology proceedings: Morgantown, WIJ, w.v. Geol . and t.con . Survey, p. 55-60. The Pickaway Limestone generally contai�s 30-50% insolubles , as compared to a 15% average for the Union Limestone . The effect on cave developoent is as expected . The Pickaway contains few and very small caves compared to the Union. Even the elliptical partings, which one might expect to facilitate cave development, do not seem to aid solution at all.

Hess, J. W. , 1976 , A review of the hydrogeology of the Central Kentucky Karst: NSS Bulletin, v. 38 , p. 99-102. Brief, general SUIII!Iary of hydrogeology of the area. Four types of catchments, plus river backflooding, supply recharge to the basal springs : sinking streams, sinkhole areas, perched aquifers, and karst valleys . Ve rtical shafts rapidly transmit water downward through the vadose zone . The water table has a relatively high gradient of 9.9 �under the Sinkhole Plain and a relatively low gradient of 0.5 �under the Chester CUesta. Its shape is determined by shale layers in the lower part of the caverr,ous limestone .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hess, J. ¥. , and Harn�n , R. s. , .9ol , Geochronology of speleothems from the Flint Ridge-Mai!IOOth cave sy;;·.:em, Kentucky, U.S.A. , in Beck , B. F. , ed ., Eighth International Congres\ of Speleology Proceedings : Huntsville, AL, NSS, p. 433-436. Th230/U234 dates on massive flowstone deposits in passages greater than 550 ft in elevation indicated that these passages and their deposits are greater than 350,000 yr old. Smaller flowstone deposits from various portions of the cave yield finite ages in the range 7,000 to 250,000 yr BP. A flowstone carapace on a sediment bank in Mud Avenue , the lowest accessible portion of the cave at 470 ft, dated at 140, 000 yr BP, suggesting that the lowet levels of the cave system are young, most likely developed during the last two glaciations .

Hewett, D. F. , 1916, Same manganese mines in Virginia and Maryland : U.S. Geological Survey Bulletin, v. 640-C, p. 37-71. Relates manganese residual ore deposits to the erosional history of the area. No sections shown.

Hewett, D. F. , and Crickmay, G. w. , 1937, The warm springs of Georgia, their geologic relations and origins, a summary report: u.s. Geological Survey Water-Supply Paper, v. 819, 40 p. The water of wa rm Springs is that which falls on the crest of Pine Mountain and is carried in the Hollis Quartzite to a depth of about 3000 ft so that it absorbs heat from the rocks and is delivered at the surface with a temperature of 88 degrees F. Figure 1 is a geological cross section of the area, showing route of the water.

Hickok , W. 0. , 1933, Erosion surfaces in south-central Pennsylvania: American Journal of Science , v. 225, p. 101-122. Uses the method of projected profiles to display erosion surfaces. Longitudinal gradients of streams show knickpoints not related to lithology. Attempts to correlate terraces of Susquehanna River. Infers the existence of a large numbe r of partial peneplains. Elevation� of wind gaps appeared to coincide with those of the erosion surfaces.

Hill, c. A. , DePaepe , D., Eller, P. G. , Hauer, ':>. M. , Powers, J. , and Smith, M. 0. , 1981, Saltpeter caves of the United States: NSS Bulletin, v. 43, p. 84- 87. Contains map showing distribution of limestone caves containing saltpeter deposits.

Hinson, H. G. , 1965, Floods on small streams in North carolina, probable magnitude and frequency: u.s. Geological Survey Circular, v. 517, 7 p. The mean annual flood (Q 2.33) is related to drainage area (A) by the following equation: Q 2.33 - GA to the 0.66 power, where G, the geographic factor, is the product of a statewide coefficient (115) times a correction which reflects differences in basin characteristics.

Hitchcock , c. H. , 1885, The recent landslide in the White Mountains: Science , v. 6, p. 84-87 . Describes the OWl 's Head landslide of July 10, 1885, which travelled 1.5 miles.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hobbs , W. H., 1904 , Lineaments of the Atlantic border region: Geological Society of America Bulletin, v. 15, p. 483-506 . Mainly concerned with joints and other fractures, but t.here is some discussion of effects on stream drainage patterns .

Hocutt , c. H. , 1979 , Drainage evolution and fish dispersal in the central Appalachians : Geological Society of America Bulletin, Part II, v. 90, p. 197-234. Bas� � on the distribution of fi sh species, author argues for major changes in drainage system of Teays River in late Cenozoic, involving major captures and a westwa rd retreat of many kilometers of the Atlantic/GUl f drainage divide . Provides maps of hypothesized changes. Also see stmmary in GSA Bulletin Part I, p. 129-130.

Hocutt, C. H., Denoncourt, R. F. , and Stauffer, J. R., Jr., 1978, Fishes of the Greenbrier River, West Virginia, with drainage history of the central Appalachians: Journal of Biogeography, v. 5, p. 59-80. During glacial blocking of the Teays drainage, faunal exchanges between the Teay , and adjacent drainages facilitated the dispersal of Mississippi basin derived fish stock . Due to the competitiv.e advantage of Atlantic slope streams, the Mississippi River/Atlantic slope divide migrated west via stream captut·es . Some of the Teays drainage was captured by the evolving Roanoke/James river systems . Mississippi basin fish species thereby reached Atlantic streams.

Hodgson , D. A. , 1967, The morphology of an area of patterned ground in central Pennsylvania [M.S. thesis] : University Park , PA, Pennsylvania State Un iversity, 62 p. Figs. 5-7 show base map of patterned ground - shrub-covered fines vs . open blocks. Found no preferred orientation of blocks. Likewi se , found no systematic variation in block size. Found that patterns change and percent of area in vegetation decreases with increase in slope angle. on slopes of 15-20 degrees, zones of exposed blocks are divided by islands or strips of shrubs on ' �ser gradients. At 10-15 degrees, blocks show a tendency to concentrate in shallow, irregularly spaced channels, perhaps 2-3 ft below veg . areas. At 5-10 degrees, an anastomosing pattern is seen, with stone stripes or streams surrounding islands of veg . At 0-5 degrees , stripes tail off into an extensive shrub cover with isolated stone pits. The shallow channels continue .

Holden, R. J. , 1938, Geology of Mountain Lake , Virginia [Abstract ]: Virginia Academy of Sciences Proceedings, v. 1937-38, p. 73. Author notes that although the upper Martinsburg shows no lime on its outcrop near the lake, it has abundant impressions of fossils which were originally limy, and in the New River gorge it has many beds which are conspicuously limy, showing 50 percent solubility. This solubility and the thickness of the upper Kartins�rg are adequate to explain th� depression represented by Mountain Lake .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hollingsworth, T. J., 1977 , Spheroidal weadhering of f�.dstones in Nichola� County, west Virginia [M.S. thesis]: Morgantown, wv, university of We st Virginia, 84 p. By sampling a spheroid along a single bedding pbne from the core to the highly weathered outer shells, it was possible to study the various stages of weathering. weathering processes examined inc�:�e the breakdown uf non-resistant minerals such as feldspars and carbonates, migration and deposition of iron oxyhydroxides , and the alteration and expansion of argillaceous materials. Results indicate that sphe roidal �athering is caused by the expansion of argillaceous materials.

Hollyday , E. F., and Goddard, P. L., 1979, Channel characteristics identify losing �tream reaches [Abstract]: u.s. Geological Survey Professional Pape r, v. 1150, �· 118. The cha."Ulels of losing strea11 reaches in limestone areas are characterized by banks that are steep and higher than the streambed is wide, large amounts of flood trash in the center of the channel , tightly compacted and poorly sorted bed and bank material, and trees or grass in the center of the channel .

Holmes, c. D., 1964 , Equilibrium in humid-climate physiographic processes: American Journal of Science , v. 262 , p. 436-445. Author argues that the Piedmont Plateau is a dissected peneplain.

Holmes, J. A. , 1899, General physiograrhic features of North Carolina: North Carolina Department of Conservation and Development Bulletin, v . 8, p. 20- 25, 68--88, 180. Brief description of physiography of North carolina.

Holmes, J. S., 1917, Same notes on the occurrences of landslides : Journal of the Elisha Mitchell Scientific Society, v. 33, p. 100-105. Describes Jebris avalanches of July, 1916. Notes due to overrunning of level land, some areas are ccvered with from 1-3 ft of a subsoil of thoroughly decCXDpOsed rock. More slides occurred on SE, E, and W slopes, with fewer on N, chiefly due to IID..lch greater depth of decomposition of rocks on southerly slopes. Most of larger slides occurred in slight hollows .

z. Hoes, A. B •. and Bailey, c. , 1986, Reconnaissance of surficial geology, regolith thickness, and configuration of the bedrock surface in Bear Creek and union valleys, near oak Ridge , Tennessee : u.s. Geological Survey water Resources Investigations Report, v. 86-4165, 1 p. Analysis of driller's logs and lithologic logs andco mparison of these data with a topographic map indicate that topography and depth of weathering < re interdependent and are ultimately controlled by lithology. Topographic patterns were therefore used to extend localized geologic data. Maps of the geology, thickness of regolith, and configuration of the bedrock surface are presented. On thickness map, intervals are 0-10, 10-20, 20-50 , and 50-75 feet. Regolith thinning in proximity to major streams is indicated. Rock types include Rome Formation, Ma�;ville Limestone , �olichucky Shale, Maynardville Limestone , and Coppe r Ridge Dolomite.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hoove r, M. T., 1983, Soil development in colluvium in footslope positions in the Ridge and Valley physiographic province of Pennsylvania [Ph.D. thesis] : University Pa rk, PA , Pennsylvania State Univers\ty, 271 p. Colluvial soils wer( investigated to depths of 3-4 m in foo� slope positions along 4 llldjor ridges . Landforms include t ock-ar!OClrecl solifluction lobes and terraces . Observed a parent mat·�rial stratigraphy of 3 upper brown layers, a red layer, and an underlying brown layer. The red layer was a tl-uncated in s.;.tu pr�isconsin p3leosol with 5YR 5/6 to 2.5 YR 5/8 colors, highly wea�hered sandstone rock fragments , truncated, buried and compacted plleoargillic horizons, and stone lines. Author suggests that there have been multiple periods of colluviation associated with cold glacial environmentE. that alternated with periods of landscape stability.

Hoover, M. T. , and Ciolkosz, E. J., 1988, Colluvial soil parent �terial relationships in the Ridge and Valley physiographic provi��e of Pennsylvania: Soil Scienc� , v. 145, p. 163-172 . In footslope positions studied, much of the coll\!Vi'i.llll cc•nsi�ts of an upper brown layer (UBn layer) ove rlying a ru. ried rt!d layer (RdJ . Landforms present at the study area indicate that the UBn laye� accumulated 'lS stone-bank!:d solifluction lobes or benches that flowed ove!" .. 'lle Rd layer during a periglacial climate . The UBn layer has 1� rt to 7.5 YR hues, is yenerally 1 to 3mthi ck , and can be separated into sublayers. The Rd layer hz.s mostly 5 YR hues and is 1 to 2+ m thick . The coloring of the Rd la� er is related to weathering rather than lithology. Beneath the col:l.uvium is a thin lower brown layer (LBnlay er) of residuum over bedrock . The lateral continuity of the layers allows proposal of a parent-material stratigraphy for colluvium in these !oc ' slope positions.

Hopson , c. A. , 1958, Exfoliation and weathering at Stone Mountain, Georgia, and their bearing on disfigurement of the Confederate Memorial: Georgia Mineral Newsletter, v. 11, p. 65-69 . Pr ovides general discussion of exfoliation. Map showin� joints, sheet structure, foliation, and other structural features is given. Discusses and ;;hows pictures of Pxpansion cracks. Also discuss�s annular weathering pits, and effects on Confederate Memorial.

Houser, B. , 1980, Erosional history of the New River, southern Appalachians , Virgi"ia [Ph.D. thesis ]: Blacksburg, v.A, Virginia Polytechnic Institute , 226 p. httempts to date higher-level New River alluvium by means of zircon/tourmaline ratios, using simplifying assumptions . Discusses possible drainage evolution of New River. Notes that most high-level alluvium is preserved ove r carbonate raL�er than clostic bedrock .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Howard, A. D. , 1968 , Stratigraphic and structural c�ntrols on landform d�velopment in the Central Kentucky Karst: NSS Bulletin, v. 30, p. 95-114. The number of sinks and hilltops un Meramec and lowest Chester rocks was found to be closely controlled by the stratigraphic horizon upon which they are developed and the local and regional structure . Several persistent sink-forming stratigraphic units were found in the basal Ste . Genevieve and uppe r St. Louis formations . The form of the Dripping Springs escarpment is closely controlled by the stratigraphic dip; low dip is associated with an irregular escarpment front and with solutional valleys below the escarpment .

Howard, A. D. , and Smith, D. D. , 1956, Studies bearing on erosion surfaces in the u.s. and Canada , 1952-1955 - a review, in 18th International Geographical Congress, Commission for the Study and Correlation of Erosion Surfaces, 8th Rpt ., Pt. 4: International Geographical Union, p. 54-66 . Authors review 11 papers dealing wi th erosion surfaces in the Atlantic drainage .

Howard, J. L. , and Amos, D. F. , 1981, Geologic and pedologic evidence of six surticial stratigraph�c units in the Richmund, Virginia area [unpub . manuscript, VPI Departmen _ of Ag ronomy] : Blacksburg, VA, Vi rginia Polytechnic Institute, 171 p. Discusses in detail a chrunosequence of soil series with physical , chemical , and muneralogical properties that show increased weathering with height above the�ames River.

Hoye r, M. C. , 1976, Quaterr�ry valley fill of the abandoned Teays drainage system in southern Ohio [Ph.D. thesis]: Columbus , Ohio, Ohio State University, 185 p. See abstract below.

Hoye r, M. C. , 1983, Sediments of the Te lys drainage system in southern Ohio [Abstract]: Geological Society of .\merica Abstracts with Programs, v. 15, p. 600 . Based on the sedimentary features and the regional distribution, the Minford clay was deposited in a single episode , probably as a lacustrine deposit resulting from the damming of the Teays drainage system by the first Laurentide ice sheet to reach the west-central Ohio or central Indiana area. Abandonment of the Teays system followed. Minfo�d clay shows reversed magnetism.

Hubbard, D. A. , and Holsinge r, J. R. , 1qa1 , Karst development in the Front Royal 7.5 minute quadrangle of Virginia, in Beck , B. F. , ed ., Eighth International Congress of Speleology Proceedings : Huntsville, AL, NSS , p. 511-514. Authors briefly discuss geologic and geomorphic control of karst d�velopment in part of the Shenandoah Va lley.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hubbard, D. A. , and Holsinger, J. R. , 1981, Karst development in Rye Cove , Virginia , in &eck , B. F., ed ., Eighth International Congress of Speleology Proceedings : Huntsville, AL, NSS, p. 515-517 . Authors discuss lithologic and structural control of karst development in the southwestern part of the Valley and Ridge province .

Hubba rd, D. A. , Jr. , 1983, Selected karst features of the northern Val ley and Ridge province, Virginia [Map] : Virginia Department of Conservation and Economic Development, Division of Mineral Resources, Publication. v. 44 , 1 p. Map showing sinkholes and cave entrances in northern part of Valley and Ridge in Virginia, with short discussion .

Hubbard, G. D. , and Croneis, C. G. , 1924, Notes on the geology of Giles County, Virginia: Denison University Bulletin, Jour. Sci . Lab. , v. 20, p. 307-377 . On p. 312-314, authors interpret topography of Giles county as the product of four erosion cycles.

Humbertson, P. G. , 1. 977, Va lley morphologies related to process dominanc:e in the uppe r Allegheny [Ph.D. thesis]: Pittsburg, Unive�sity of Pittsburg, 167 p. In nori:h-central Pennsylvania and southwestern Ne\. York , author divided stream valleys into four groups: 1) unaffected by glaciation; 2) affected only by pre-Illinoian glaciation; 3) affected �f Illinoian and earlier glaciation; 4) affected by Wiscons�n and earlier glaciation. Then she measured valley width, depth, longitudinal gradient, plan expression of channel, and the slope of valley walls, and compares the different types of valleys .

Hunt , C. B. , 1967, Appalachian Highlands, in Hunt , c. B. , ed ., Physiography of

the United States: San Francisco, W.H. Fr.eeman and Co ., p. 166-204 . Author provides a brief account of Afpalachian physiography, with some nice sketches and diagrams.

Hunt, c. B., 1972, GeolQgy of soils: San Francisco, W.H. Freeman and Co., 344 p. Contains scattered reference to examples from Appalachians , such as Fig. 4.7 showing cuestas on Piedmont , Fig. 5.3 showing average summer ground temperature at depths of 2 ft, p. 152 showing sketch of saprolite in Piedmont , Fig. 7.16 showing Bauxite areas, Fig. 9.5 showing alluvium overlapping saprolite, Fig. 9.12 showing relation between saprolite, alluvium, and groundwater .

Hunt, C. B. , 1974, Natural ragions of the United States and Canada : San Francisco, W.H. Freeman and Co. , 725 p. Chapter 11, the Appalachian provinces, is quite relevant, as are scattered references, such as Fig. 8.20 showing dwarfed vegetation on Serpentine formation, Fig. 10.13 showing sketch of upland .dver gravel, Fig. 10.14 showing cross-sections of the Potomac River valley .

Hunt , c. B. , 1977, Surficial geology of :he United States : Explanation to accompany the 1:7,500,000 scale map: u.s. Geological Survey Open-file Report, v. 77-232 , 7 p. Rough map of surficial deposits of the u.s. together with very brief descriptions of the deposits.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Hupp , C. R., 1983, Gee-botanical evidence of late Quaterna� mass wasting in block field areas of Vi rginia: Earth Surface Processes and Landfonms, v. 8, p. 439-450. Several block fields were investigated for evidence of recent movement using the degree of lichen growth, differences in block weathering, and rock-fall damaged trees. High flows on Pas�age Creek coincidec with tree-ring determined dates of block-field movement.

Hupp , C. R., 1986 , The headward extent of fluvial landfonms and associated vegetation on Massanutten Mountain, Virginia: Earth Surface Processes and Landforms, v. 11, p. 545-555. The relations among channel gradient, basin area, stream order, and the headward extent of fluvial landforms and vegetation was studied in 18 small basins and larger nearby streams. Low-order streams were traversed to their basin heads . Notice was made of the point or region of the disappearance of fluvial landforms . Indicator species were used to confinnlandfonn identification. Results suggest that gradient is the most important factor controlling the development of flu�ial landforms. Floodplains have not developed along stream reaches where average channel gradients exceed 0.15. �q el shelves and associated vegetation occur farther upstream than floodplains.

Hupp , C. R., and Osterkamp, W. R., 1985, Bottomland vegetation distribution along Passage Creek, Vi rginia, in relation to fluvial landforms: Ecology, v. 66 , p. 670-671 . Persistent distribution patterns of woody vegetation within the bottomland forest were related to fluvial landforms, channel geomet�, streamflow characteristics, and sediment-size characteristics. Distinct species distributional patterns were found on four common fluvial geomorphic landforms : depositional bar, active-channel shelf, floodplain, and terrace . Vegetation patterns appear to cevelop more as a result of hydrologic processes associated with each fluvial land:orm rather than from sediment-size characteristics. r:.ood disturbance may be an important factor in maintaining tne vegetation patterns.

Hupp , C. R. , and SigafooE , R. S., 1982, Plant growth and block-field move��nt in Vi rginia: u.s. Forest Service General Technical Report, v. PNW-141, p. 78- 85. Similar to Hupp's 1983 paper .

Huppert, G. , Wheeler, B., and Knox , L. , 1983, Suburban expansion and sinki1ole flooding: A case study from Tennessee, in Doughe rty, P. H., ed ., Envi ronmental karst: Cincinnati , GeoSpeleo Publications, p. 15-23 . Briefly describes sinkhole flooding that inundated houses in Coc�eville, Tennessee, and attempts to relate the flooding to changes in landuse .

Hursh, C. R. , 1941, The geomorphic aspects of mudflows as a type of accelerated erosion in the southern Appalachians [Abstract): u.s. Forest Service Research Paper, v. SE-93, p. 23. Briefly notes impor�ance of mudfl�NS on slopes in the southern Appalachians.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ireland, H. A. , Sharpe, C. F. s., and Eargle , D. H. , 1939, Principles of gully erosion in the Piedmont of South Carolina : U.S. Department of Agriculture Technical Bulletin, ·r. 633, 142 p. The correlation of rock type with soil series and erosion hazard is particularly close in the Piedmont . The red and yellow soils are characterized by profiles in which the B horizon is more resistant to erosion than the underlying parent material (i.e., saprolite). Authors describe 4 stages thr:rugh which gullies 30 . They reconstructed the histories of 6 gully areas by means of physiographic, ecologic, and human evidence .

Isphording, w. C. , 1981, Mineralogical evidence for a Miocene Gulf of Mexico outlet for the ancestral Tennessee River [Abstract): Geological Society of America Abstracts with Programs , v. 13, p. 10. The common occurrence of garnet , epidote , clinozoicite, horn blende , plagioclase, and potash feldspar in Miocene sediments of the Hattiesburg Formation in Perry County can only be explained by calling upon a Piedmont source of moderate-rank , metamorphic rocks. The presence of a major river draining southwesterly across Mississippi would help to explain a numbe r of anomalies in the surficial geology of southern Mississippi .

Itter, H. 1'1.. , 1938, The geomorphology of the WyOJning-Lackawanna region : Pennsylvania Topographic and Geologic Survey Bulletin, 4th series, v. G-9, 82 p. Discusses erosion cycles and effects of glaciation in this region in northeastern Pennsylvania. Describes terraces of the Susquehanna River.

Jacobson, R. B., 1986, Spatial and temporal distr�Uutions of slope processes in the upper Buffalo Creek drainage basin, Marion County, We st Virginia [Ph.D. thesis): baltimore, Johns Hopk ins t�iversity, 484 p. The last extensive climatically-induced slope instability in the area occurred in the early Wisccnsin, during which thick diamicton colluvium ('IDC) was deposited on slopes; large volumes of 'IDC remain stored in zero-order tributari�s today. Woodfordian-age alluvial fans attest to renewed, milder i�stability in the late Wisconsin. Th� Holocene to Recent history suggests that slope failures, which are the ultimate sediment s�Jrces, are sufficiently scatte�ed in time and spa�e that the alluvial system receives sediment at a steady rate . A tree-ring dated , 33-year record of slope failure provides a basis for calculating a magnitude-frequency product curve showirg that long wet periods (measured as 30-day runoff) with return intervals of approximacely four :pars are responsible for the most. aggregate geomorphic work on these slopes . A calibrated failure model predicts at-a-site failure recurrence of 1800 to 4300 years.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Jacobson , R. B. , Genesis and distribution of colluvium in the Buffalo Creek area, Marion County, We st Vi rginia: Transportation Research Board Proceedings , in press. Two types of colluvium - thick deposits of ent renched , diamicton , debris-flow generated colluvium occur as long fingers in zero-order drainage basins . These deposits are the product of early Wisconsin slope processes that produced colluvium at a greater rate than it could be removed by streams. The second type is generated as modern slope failures shear bedrock and transport material downslope . It collects on bedrock benches until failure conditions are reached, "nere•.1pon it is transferred to the next lower bedrock-co�trolled bench.

Jacobson, R. B. , and Coleman, D. J., 1986 , Stratigraphy and recent evolution of Maryl&1d Piedmont flood plains : American Journal of Scienc� , v. 286, p. 617-637. Floodplains in 9 reaches of 7 small Maryla� Piedmont streams (drainage area 10.6 - 215.0 square kilometers) show 3 distinct stratigraphic units deposited during 3 periods of different hydrology and sediment supply . Before 1730, thin, fine ove rbank sediments were deposited on top of thin laterally-accreted sands . From 1730-1930, thick. fine ove rbank sediments and thin lateral accretion sands were depos2ted. After 1930, there was a slight decrease in water yield and a substantial decrease in sediment yield; streams accomodated these changes by altering the floodplain formation process to one of lateral accretion of sand and gravel while removing a large volume of fine sediments from floodplain storage .

Jacobson , R. B., Cron, E. D. , and McGeehin, J. P. , 1987 , Preliminary results frcm a study of natural slope failures triggered by the storm of. Novembe r 3-5, 1985, Germany Valley, West Virginia and Virginia [Extended abstract ]: u.s. Geological Survey Circular, v. 1008, p. 11-16 . The type and number of slope failures triggered by the storm were strongly controlled by the underlying lithology; fine-grained residuum from the Martinsburg Shale and some Ordovician carbonates were more susceptible to fa:lure under conditions of this low-intensity storm than were colluvium and residuum of the sandier lithologies. Slumps and sl�flows on fine-grained regolith are smaller but more numerous than the rare, large debris avalanche-debris flnws on the sandier lithologies. A slope-aspect preference is not readily apparent . Dip slopes seem more susceptible on the Tuscarora than are scarp slopes. Slope failure density increases with increasing storro-total rainfall along a transect where lithology and structure are constant .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Jacobson, R. B., Elston, D. P. , an1 Heaton, J. w. , 1988 , Stratigraphy and magr.etic polarity of the high terrace remnants in the upper Ohio and Monongahela Rivers in West Virginia, Pennsylvania, and Ohio: Quaternary Research, v. 29, p. 216-232 . Stratigraphic evidence indicates a correspondence between terrace histories in the ancient Teays and Pittsburg (proto-Monongahela) drainage basins. Fou r terraces are id�ntified in each. Sediments of the lower three alluvial and s1ackwater terraces, correlated with Illinoian, early Wisconsin, and late Wisconsin glacial deposits, have been traced al0ng the modern Ohio River through the formPr divide between the Teays and Pittsburg systems. Some deposits of the highest slackwater terrace in both the Teays and Pittsburg basins hav� reversed remanent magnetic polarity. This restricts thl! age of the first ice-

Jacobson, R. B. , McGeehin, J. P., and Cron, E. D. , 1987, Hillslope processes and surficial geology, Wills Mountain anticline, West Virginia and Virginia , in Kite, J. S., ed., Research on the late Cenozoic vf the Potomac highlands : SE Friends of the Pleistocene, p. 31-55. Consists of 2 parts. In first, authors attempt to determine factors controlling the temporal and spatial variability of the 1985 slope failures. l�f:Eectiveness of storm apparently steli1IIed from its duration. Most failures were in colluvium and residuum of Martinsburg Formation . All 5 large debris flows, however, were initiated in TUscarord sandstone residuum or weathered bedrock . The bouldery Tuscarora colluvium appears to have greater shear strength than that along bedding planes and fractures in the weathered bedrock . Suggest that those lithologies that are infiltrated and drained quickly will be susceptible to fai.lures triggered by high-intensity, short-duration rainfall ar� those that are infiltrated and drained slowly will be susceptible to failure triggeree by low-intensity, long-duration rainfall. Second part concerns mapping and interpretation of surficial geology. Uses ranges of erosion rates to ��lculate that the sandstone at the crest of the anticline was br�ached between 205-14 Ma go a and the highest debris terraces on �vur ridges ·� re deposited 7.3-0.5 Ma ago. Map includes 4 l�vels of debris terraces, thick and thin colluvium. Points out importance for landform evolution of deposits that are more resistant to erosion than bedrock .

James , w. R. , and Krumbein, W. C., 1969, Frequency distributions of stream link lengths : Journal of Geology, v. 77, p. 544-565. A topological study of stream link lengths with data obtained from the Inez quadrangle, Kentucky .

Jameson, R. A. , 1981, nevelopoent of f:;.ow routes and cave passages from fault segments in West Virginia caves, in Beck , B. F., ed. , Eighth International Congress of Speleology Proceedings: Huntsville, AL, NSS, p. 717-719. Structural segments formed by minor reversP. faul ts are abundant in MiRsissippian limestones. The faults tend to form ramps with "S-shaped" cross sections . This study illust:ates the most c011100n developoental sequences on fault segments.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Janssen , R. E. , 1952, The history of e. river: Scientific American , v. 186, p. 74-80. A popular account of the d:ainage evolution of the Teays River system.

Janssen , R. E., 1953, The Teays River: Ancient precursor of the east : Scientific Monthly, v. 77, p. 306-314. Popular account of the Teays River and its evolution.

Jenkins , C. T. , 1960, Floods in Tennessee : Ma�1itude and frequency: Nashville, Tennessee Department of Highways , 68 p. Flood magnitudes of selected frequency on unregulated strear.s can be estimated from the size and location of the drainage basil�. The effects of va riations in main-channel slope , basin shape , and size of noncontributing drainage area are negligible

Jillson, w. R. , 1919, The migration of the headwaters divide of Right Middle Creek, Floyd County, Kentucky: American Journal of Science , v. 47, p. 60- 64 . Suggests that Right Middle Creek has shifted its divide 8 to 10 miles north-westward and has captured the headwaters of the Burning Fork of Licking River. The extent of the capturF.o area is about 20 square miles .

Jillson , w. R. , 1927, Major drainage modification of the Big Sandy River [Abstract ]: Kentucky Academy of Sciences Transactions 1924-1926 , v. 2, p. 137-139. !arge quartzite boulders indicate that the ancient Big Sandy River had its headwaters in the Roan Mountain region of western North carolina . Headwater piracy of the Clinch and the Blue Stone Rivers operating advantageously along northeast and southeast lines of favorable structure beheaded the upper one-fifth of Big Sandy River.

Jillson, w. R. , 1928, Peneplains in Kentucky: Pan-American Geologist, v. 50, p. 333-338. Plate 18 is a map of Cretaceous and Tertiary pe��plains and deposits in Kentucky .

Jillson, w. R. , 1950, American fluvial Pliocene deposits bordering the western margin of the CUmberland Plateau, in Eighteen�� International Geological Congress, Part IX, Proceedings of Section H, the Pliocene Pleistocene Boundary: International Geol ogical Cc�gress, p. 54-58 . The major westerly and northwesterly flowing tributarie� of the Ohio River have entrenched themselves into the l'lid-Tert.iary pcnepl�in [i.e , the Highland Rim peneplain) to levels ranging from 350 to �10 ft A.T. Old high-level gravel deposits are found at levels varying from 700 to 950 ft ; they grade gradually downstream into the Lafayette formation.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Jobling, J. L., 1969, The origin of sh�le chip deposits in southeastern Centre County , Pennsylvania [M.S. thesis]: Univerrity Park , PA , Pennsylvania State University, 51 p. Describes petrology and occurrence of shale-,�hip c.olluvium. Notes preferentially developed on southeast slopes. Thinks oriqinated as sol1fluction. C�res to grezes litees .

Johnson , D. W. , 1905, The distribution of freshwater faunas as an evinence of drainage modifications : Science , v. 21 , p. 588-592 . Johnson argues against using the fact that Unionidae mollusc shells occur in both the Tennessee and Coosa drainage as evidence that the Tennessee must have been divered from a former southward course by capture near Chattanooga . Notes that Darwin observed that young molluscs just hatching will attach themselves to the feet of a duck and remain alive in this position out of water from 12 to 20 hours.

Johnson , D. w. , 1905, The Tertiary history of the Tennessee River: Journal of Geology, v. 13, p. 194-2.11. Argues against diversion of the Tennessee River from a southward course we£;tward by r.apture. Ra�.he r, Johnson believes that river acquired its course across the mountains some time before the close of the Cretaceous Period of baseleveling. Lists evidence for and against each hypotheses. Attacks t:nionidae muss�! evidence . Figures 2 and 3 show Walden Ridge during Appalachian River time and at present .

Johnson , D. w. , 1907, Drainage modifications 1n the Tallulah district: Boston SOCiety of Natural History Proceedings , v. 33, p. 211-248 . Notes two peneplain levels separated by a marked escarpment . Propos�s a history of river capture for the area . Reports high-level gravels south of Tallulah Fllls. Several pe�spective sketches. Attacks evidence of capture from mussel shells.

Johnson , D. w. , 1931, Stream sculpture on the Atlantic slope , a study in the evolution of Appalachian rivers: New York , Columbia University Press, 142 p. Argues that southeast-flowing master streams of the Appalachian slope inherited their courses from a coastal plain cover which reposed upon a peneplain surface of pre-Schooley age and which �ormerly externed from 125 to 200 miles northwest of the present coastal Plain boundary.

Johnson , D. w. , 1931, A theory of Appalachian geomorphic evolution: Journal of Geology, v. 39 , p. 497-508 . Basic?.lly is .a s�..�t��ary of Johnson's book. Arg'Jes that a southeast-flowing consequent drainage system was originally superposed on AppaJ--hian structures from an ancient coastal plain cover which extended from 125 to 200 miles northwest of the present inner margin of the Atlantic �oastal plain.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Johnson, D. W. , 1933, Evolution of the drainage system of eastern NorUh America, in International Geographical Congress , 13th, Pa ris, 1931, Compces Rendus , Section 2, p. 600-606 . Johnson here summarizes the thesis put forth in his 1931 book , �hat the present drainage of the Appalachians is the result of supe rposition from an extensive cove r of coastal-plain sediments .

Johnson, D. w. , 1939, Biologic evidence of capture : Journal of Geomorphology, v. 2, p. 86-91 . Au thor says that to use mussel distribution as evidence of former course of river, must establish that mussels requi re direct fresh-water connection between the two streams in order to pass from one to the other, and this has not been demonstrated.

Johnson , D. w. , 1941 , Mussel distribution as evidenc� of drainage changes , part I: Journal of Geomorphology, v. 4, p. 307-321 . Attacks in detail concept th�t mussel distribution can be used as evidence of stream drainage changes.

Johnson , D. w. , 1942, Mussel distribution as evidence of drainage changes : Journal of Geomorphology, v. 5, p. 59-72. Continues attack on concept that mussel identification can be used as evidence of stream drainage changes.

Johnson, D. w. , Bascom, F. , and Sharp, H. S., 1933, Geamorph0logy of the central Appalachians, in Sixteenth International Geological Congress Gu idebook 7, Excursion A-5: International Geological Congres�o: . 50 p. Guidebook to many a�eas rliscussed in previous Johnson papers.

Johnson, G. H. , and Goodwin, B. K., 1967 , Elliptical depress1ons on und1ssected highland gravels in northe•n Chesterfield County, Virginia [Ahstract): Virginia Journal of Science , v. 18, p. 186 . Numerous elliptical to subr :L�- :-: depressions are found on undissected gravel uplands nea: ri jdJ ct.'i.:n, Virginia. The deeply weatl,ered quartz gravel and �:.< �j. in ,.,f.i : the t.asins occur, overlie Triassic arkoses and �,_: l�s "' i ···: anitic rocks of the Piedloc;nt . Basins range fr0111 \.1 • t'-' .; e .tile long . Age and origin unknown .

Joh�son , R. A. , 1983, Stre� channel response to extreme rainfall events : The Hurricane Camille Storm in central Nelson County, Vi rginia [M.S. thesis): Charlottesville, VA, university of Virginia, 109 p. Measured bankfull channel widths before and after Hurricar.? Camill� using ae�ial photos . �b en regressed percent increase in ch;�el width against numerous morphometric and other variables on p. 10 . was abJ.e to explain 82% of tha variance in channel-width incr�ase .

Johnston , w. D. , Jr •• !930, .'hysi cal divisions of northern Alabama: Alabama Geological Survey Bul letin, v. 38 , 48 p. Describef major areas withl� each phjsiographic province .

Johnston, W. D. , Jr. , 1932, A revi sion of physical div�sions of northern Alabama: Washington Academy of Sci.en-:es Journal, v. 22, p. 220-223. Author modifies his 1930 physiographic divisions of nc rthern Alabama.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Jones, w. K. , 1973, Hydrology of limestone karst ln Greenbrier County, We st Virginia: west Virginia Geological and Economic Survey, v. 36 , 49 p. Dye-tracing and other techniques showed that the di rection of subsurface flow was frn'.!'.d to be generally independent of the topography . Flow paths cross under surface ridges and often trend opposite to surf;::�e slope . The ove rall di rection of flow routes is toward lower base level streams, but is influenced locally by variations 1n geologic structure, lithology, vegetal cover, climate , former surface and subsurfa�e flow paths , and the length of time the aqui fer had unde rgone develoiXMnt .

Jones, w. K. , 1983, Karst hydrology in West Vi rginia, in Medville, D. M. , Dasher, G. R. , and werner, E. , eds., Guidebook for the 1983 Na tional Speleological Society Convention, Guidebook 23: Morgantown , wv, West Virginia Speleological Survey, p. 25-34, A popular summary that tries to characterize the karst hyd rology in each district of west Virginia.

Judson, S., 1975, Evaluation of Appalachian topography , in Melnorn, w. N. , and Flemal , R. C. , eds. , Theories of landform developnent : Boston, Allen & Unwin, p. 29-44. Author shows implications of modern plate-tectonics theory for long-term drainage evolution i� the Appalachians . Orogeny beginning in Ordovician resulted in northwesterly drainage through the Jurassic. The northwestward regional tilt was reversed to the southeast as the continental margin subsided as a result of the divergence of the N American plate from the spreading center now in the Mid-Atlantic ridge . Beginning with that reversa�. the JOOdern drainage has developed as streams adjusted tl�mselves to a changing base level L1 ways outlined by i':.M. Davis and others.

Jurkowski , G. , and Re ilinger, R. , 1981, Recent vertical crustal movements: The eastern United States [NUREG/CR-2290): washington, DC, Nuclear Regulatory Commission, 74 p. Significant elevation changes have been identified in a numbe r of areas along the east coast of the u.s. , in the New Madrid seismic zone , and elsewhere . Uplift of the Appa lachians , doming of the Adirondack Mountains, localized deformation near the Brevard fault zone , and eastward tilting of the Atlantic Coastal Plain are more problematic because of possible systematic errors.

Kalisz, ?. J. , 1986, Soil properties of steep Appalachian old fields: Ecology, v. 67, p. 1011-1021. Concerned with determining the effect of shiftilig cultivation of corn on steep, mesic slopes in the Appalachians from 1800 to 1930 . Intensive sampling of the 0-60 em soil depth revealed only minor differences in the properties of formerly cult ivated vs . uncultivated soils. Suggests reason for this is that cleared fields typically were located on landscape positions characterized by favorable water regimes and by deep, porous soils with uniform physical properties throughout the rooting depth . Soils on such sites are resistant to permanent erosional degradation and are rapidly rejuvenated by processes associated with reforestation.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Kastning , E. H., Jr ., 1984 , Hydrogeomorphic evolution of kursted plateaus in response to regional tectonism, in LaFleur , R. G. , ed. , Groundwater as a geomorphic agent : Boston , Allen & Unwin, p. 351-3a2. Discusses Mississippian karst of Kentucky, among others. Cave passages are usually excavated along bedding-plane partings or fractures that are the most open initially, or are favorably oriented along prevailing hydraulic gradients . These openings will enl arge at the greatest rates and become the master cunduils. Consequently, cave passages may accentuate the �xistence of major fractures. Surface karst features tend to become aligned along ve rtically oriented fractures.

Kastning , K. M. , and Kastning, E. H., 1981, Fracture control of dol ines, caves, and surface drainage : Mississippian plateau, western Kentucky, USA, in Beck , B. F., ed. , Eighth International Congress of Speleology Proceedings : Huntsville, AL, NSS , p. 696-698. Lineaments drawn from topographic maps along very distinct doline alignments conform to r�gic�l str�ctural elements and are interpreted as highly fractured zones, many of which are not visible on aerial photography or on the ground .

Kaye , J. M. , 1974, Compositional sorting of topographically high Tennessee h'.'!" gravels: A glacial hypothesis: Geology, v. 2, p. 45-47. Metamorphic quartz and other minerals from Mississippi indicate that the Tennessee River at one time illsp ed out of its valley, following an ancestral Black �lt stream system through northeastern Mississippi . Author attributes this spillover to meltwater from Blue Ridge Pleistocene glaciers.

Keith , A. , 1895, Some st�ges of Appalachian erosion: Geological Society of America Bulletin, v. 7, p. 519-525. Appalachian degradation was marked by at least 7 periods of approximate reduction. In same cases the resulting peneplains have been warped from th-.ir origi:�al level , but the greater portion retain nearly their original attitudes. The form of any minor period would have been obliterated by a greater subsequent one , so that the record can only be expected to preser�e those which were in descending order of magnitude .

Keith, A. , 1902, Topography and geology of the southern Appalachians : Senate Document, 57th Congress, v. 84 , p. 111-123. A short popular article on the southern Appalachians , with numerous photos .

Keller, E. A. , 1975, Spacing of pools in Boone Pork and Sims Creek near Blowing Rock, North Carolina [Abstract): Geological Society of America Abstracts with Programs, v. 7, p. 505. Relates stream gradients to spacing of pools and riffles .

Keller, E. A. , 1977, Adjustment of drainage to bedrock in regions of contrasting tectonic framework [Abstract): Geological Society of America Abstracts with Programs , v. 9, p. 1046. Using Hack 's (1973) gradienL-index , compared the adju�tment of drainage to bedrock in the Appalachians with that in the San Gabriel Mountains, California.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Kemme rly, P.R. , 1975, The Port Royal, Tennessee, doline collapse - a case study : Journal of the Tennessee Academy of Science , v. 50 , p. 124-127 . The collapse mechanism was attributed to short-term dynamic loading and the modi fication of the doline to increase runoff storage capacity.

Kemmerly, P. R. , 1976, Definitive doline characteristics in the Clarksville quadrangle , Tenr.�ssee : Geological Society of Aruerica Bul letin, v. 87 , p. 42-46 . Two random samples of dolines with and without nat�ral ponds from the Clarksville quadrangle were subjected to morphometric analysis. �e twc groups are statistically different.

Kemme rly, P. R. , 1980, Sinkhole collapse in Montgomery County , Tennessee : Tennessee Division of Geology Environmental Geology Series, v. 6, 50 p. Eighteen si��hole collapses examined . The major cause of collapse appears to have been fluctuating ground-water levels.

Kemmerly, P. R. , 1980, A time-distribution study of doline collapse : Framework for prediction: Envi ronmental Geology, v. 3, p. 123-130. A temporal analysis of doline collapse indicates one approach to estimating the probability of sinki'&ole col1.apse . The distribution of collapse during one 12-month period conformed to a Poisson

distrib•�:on with a mean occurrence rate of lambda • 0.346 collap�es per week and with the interoccurrence times being exponentially distributed.

Kemmerly, P. R. , 19&!, Deline growth patterns on the western Highland Rim: Initiation to steady-state conditions: Journal of 'rhe Tennessee Academy of Sc] e�ce , v. 56, p. 12-14. Measured growth of doline over a pe•lod of several yea rs.

Kemmerly, P. R. , 1981, The need for recognition and implementation of a sinkhole floodplain hazard designation in urban karst terrains : Envi ronmental Ge�logy, v. 3, p. 281-292 . A new floorl-hazard designation termed the sinkhole floodplain is arlvocated for use by federal mortgage agencies in karst terrains so ::hat sinkhole-related flooding can be minimized. A 4-phase methodology for assessing sinkhole flood hazards in a rapidly developing karst terrain is proposed.

Kemme rly, P. R. , 1982, Spatial aP.�lysis of a karst depression population: Clues to genesis: Geological Societv of America Bulletin, v. 93, �· 1078-1086 . A multigenerational diffusion and competition process model best explained : 1) the presence of two lognormally distributed depression density subpopulations ; 2) discrete, cl�stered depression sets containing second-order �llet dolines surrounded by first-order swallet depressions; 3) geomorphic competition t� tween adjacent sP.cond-order swallet dolines for ruroff and catchment area; &m 4) a positive correlation between interdoline r;.m spacings of the small swallet order and the �:>urn of their respective major axial lengths .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 KelTIIIerly, P. R. , 1986 , Exploring a contagion model for karst-terrane f:volution : C� ological Society of America Bulletin, v. 97 , p. 619-625. The contagion karst mechanism sugge�ts that the pr�sence of one or more parent depressions increases the probability of daughter depressions developing along solution-enlarged joints that radiate outward from beneath parent depressions . As a result, sinkholes occur in clusters, consisting of a centrally located parent depression s•Jrrt.unde

Kenmcrly, P. R. , ,md Lyle, I.. , 1976, A catalog of earthquake effects on thE' western Highlo.nd Rim, ·rennessee : Journal of The Tennessee Academy of Science , v. 51 , �� 19-24. Includes gecmorrhic effects of earthquak�s .

Kemmerly, �- R. , and Towe, s. K. , 1978, Karst depressions in a time context: Earth Surface Processes and Landforms , v. 3, p. 355-361 . Used sets of aerial photographs taken in 1937 and 1972 to document aerial growth rates of sir.kholes. Aerial growth rates averaged 40, 70, and 100 square meters/century for loessial , clayey residual, and silty colluvial surficial material , respectively. Estimates of average apparent age of sinkholes, based on linear growth rates, ranged fr� 25,000 to 6S,oor yr BP .

Kerr, W. C. , 1875, Physical geography, resume , economical geology: Report of the Geological Survey of North Carolin::o., v. 1, 325 p. Describes exposures of the "gold gravels", colluvium, and organic deposits.

Kerr, w. C. , 1876, On frost drift in North Ca rolina: 'rhe Academy of Natural Sciences of Philadelphia Proceedings , v. 28 , p. 157-158. Describes colluvium in North Carolina and attributes its origin to Pleistocene cold climate.

Kerr, W. C., 1881 , On the action of frost in the arrangement of superficial earth material : American Journal of �.cience, v. 21 , p. 345-358 . Describes sections throvgh colll.vium, and attributes movement of colluvium to Pleistocene frost actio·.t.

Kerr, W. c., 1881 , Origin of S�illV new p;ints in the topography of North Carolina: American Journal of Sr.1ence , v. 21 , p. 216-219. Argues that accordance of oeaks in Blue Ridge indicates that region w-as once eroded by a gn!at glacier.

Kesel , R. H. , 1974, Insclbergs on f�e Piedmont of Virginia, North carolina, and South Ca rolina : Types and cha racteristics: Southeastern Geology, v. 16, p. 1-30 . Studied tl1e inselberg sj de-sl�� profile, the piertmont slope adjacent to it, the piedmont angle betWPen the inselberg side-slope and the piedmont sur��ce, and the thickness and characteristics of the waste cover. Grouped inselbergs into 4 types based on their association wi th or isolation from other landfoLmS.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Kesler, T. L. , 1956 , Environment and origJ � of the �•etaceous kaolin de� �sits ct Georgia and South Carolina: Econr �c Geology, v. 51 , p. 541-554 . Discusses occurrence of k�� cin in Cret3ceous coastal plain sediments . �� series rests w1confonnably on crystalline rocks, and sediment waseroa ed from p;'!dmont .

Kilgore, D. L., 1970, An historical geomorphic study of the anomalous water gaps cut in Pine Ridge-Little Mountain by the North Fork of the Holston River, southwestern Virginia [M.S. t-_t)esis] : Te rre Haute , Indiana State University, 55 p. Suggests the anomalous segments of the North Fork were produced by meanders which are either in the process ot cutting down-section thr01.1gh the Price Formation, which holds up the homorl'n al rine Ridge-Little Mountain, or have completely cut through it. In such locations the stream has gained the fr�edom to corrade laterally into the nonresistant unde rlying Devonian shale in Poor Valley on the obs�ent side of the ridge . Contains some nice block diagrams .

Kilpatrick, F. A. , and Barnes , H. H. , Jr., 1964, Channel geometry of PieC: ...... 1t streams as related to frequency of floods: u.s. Geological Survey Profes3ional Paper, v. 422-E, p. El-ElO . �le re�aL� on of the height of valley be�ches to the hei ght of water surfaces cvrresponding to floods of selected recurrence inc2tvals was inv�stigated at 34 sites. The heights of the benches were fooo" to be significantly related to the depth of flow corresponding to the mean annual flood and to the slope of the stream channel .

King, P. B., 1943, Manganese deposits of the Elkton area, Vi rgi nia : u.s. Geological Survey Bulletin, v. 940-B, p. :5-55. Describes regolith, including alluvium, and discusses pos��hle origin of residual ore .

King, P. B. , 1949, The floor of the Sl-.enancioah Valley: American Je>urnal of Science, v. 247, p. 73-93. The principal element of the floor is a series of gravel-capped benches, formed in Pleistocene time du ring alternating periods of erosion and deposition. Unconformably beneath the gravels is residual clay. Latter reaches 200 ft in thickness.

King, P. B., 1950, Geology of the Elkton area , Virginia: U.S. Geological Professional Paper, v. 230, 82 p" Describes surficial depc•sitr; in some detail . Map shows gravel-capped benches cf sevr�ral. aqes .

King, P. B., 1964, Geology of th£ central Great Smoky Mountains , Tennessee : u.s. Geological Survey Professional Pape r, v. 349-c, 148 p. On p. 130-142 describes Cenozoic deposits and landforms . Also has nice landscape sketches .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 King, P. B. , and Fergt•son , H. W. , 1960, Geology of northeasterrunost Tennessee : u.s. Geological Survey Professional Paper, v. 311, 136 p. Discusses physical geography on p. 9-11 and Cenozoic deposits and lanCiforms on pl 88-89 . Contains several cross sections of deposits and landscape sketches.

King, P. B., Ferguson, H. w. , Craig, L. c. , a�d Rodgers, J. , 1944, Geology and manganese deposits of northeastern Tennessee : Tennessee Division of Geoloqy Bul letin, v. 52, 275 p. Discusses land forms and surficial deposits on p. 41-48 . Discussion of fo�tion of the residual ore also touches on geomorphology.

King, P. B. , Neuman, R. B., and Hadley, J. B. , 1968, Geology of the Great Smoky Mountains National Park , Tennessee and North Carolina: U.S. Geological Survey Professional Paper, v. 587 , 23 p. A popular account , with little geomorphology. The re are some nice landscape sketches, howeve r.

King, P. B., and Stupka, A. , 1950, The Great Sooky Mountains - tbtH geology and natural history: Scientific Monthly, v. 71, p. 31-43. A po��lar article on the Smokjes that touches briefly on geomorphology.

Ki rkby, A. , 1965, Boulder fields on Bald Eagle Mountain, Pennsylvania [Abstract]: Association of American Geographers Annual Convention, v. 61 . Describes boulder fields . one shows some evidence that boulders can be moved by "blow-outs ." A study of tree colonization suggests this process is very slow, and that the area may not yet have been forested since the Pleistocene ended .

Kite, J. S., 1985, Depositional units on tributary floodplains in the lower Shenandoah Va l!ey [Abstract]: Geological Society of America Abstracts with Programs , v. 17, p. 98. Describes one post-settlement and one pre-settlement depositional unit. The latter may � early Holocene based on presence of boreal pollen.

Kite, J. s., 1987, Colluvial diamictons in the va lley and Ridge province , West Virginia and Virginia [ExtendP.d abstract ]: U.S. Geological Survey Circular, v. 1008, p. 21-23 . Many colluvial landforms with simple surface expression ate unde rlain by v�ry complex stratigraphies . Exposures indicate tha t different processes have dominated local slopes at di fferent times . one of the most striking attributes of colluvium throughout the central Appalachians is that many deposits are capped by a concentration of large boulders. This observation is particularly true for colluvial ap•ons . Multiple diamdctons a1 e exposed at

several localities (e.g. , Fig. 8 . 1) . A typical sequence is a thick (2-5 m) cobble-boulder diamdcton overlying a thick (>3 m) pebble diamicton . Both have strong down-slope clast fabrics and the contact between the 2 is abrupt.

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Kite, J. s. , 1987, Research on the late Cenozoic of the Potomac Highlands : SE Friends of the Pleiscocene , 85 p. This is a collection of articles dealing wi th recent research on the geomorphology of the Potomac highlands in the va lley and Ridge of West Virginia, intended as a companion to the guidebook for the fi rst annual meeting of the Southeastern Friends of the Pleistocene . TOpics include flood erosion produced by the 1985 flood, flood hydrology, slope failure, surficial geology, and maiiiiial fossils. Introduction by J.S. Kite. Individual articles dealing with geomorphology are listed separately.

Kite , J. S., and Linton, R. C. , 1987, Field guide for the First Annual Meeting of the Southeastern Friends of the Pleistocene , Canaan Valley State Park, Davis, WV, Nov . 6-8, 1987: SE Friends of the Pleistocene, 85 p. Southeastern Friends of the Pleistocene guidebook to geomorphology of northern part of Valley and Ridge in We st Virginia. Stops include Seneca Rocks, Harper Run slope failures , Judy Rlm debr is avalanche , Germany Valley overlook, Twin Run debris avalanche , South Branch flow over drainage divide, Smoke Hole reach of the South Branch -::>f the Pot(..mac , Hopeville Canyon overlook , mouth of Hopeville canyon , South Dranch Potomac River between Redman Run and Austin Run, and Dolly Sods �1e rlook .

Knechtel, M. M. , 1963, Bauxitization of terra rossa ir the southern Appalachian region : u.s. Geological Survey Professional Paper, v. 475-C, p. C151-C155. The bauxite of many deposits in the southern Appalachian region is envi saged as a product of leaching in sinkholes, wherein silica is removed from aluminiferous matter present in fill (terra rossa ) consisting of argillaceous , chert-bearing residual material . The terra rossa has resulted from earlier leaching of soluble carbonates from rocks of Paleozoic age .

Knopf , E. B., 1924 , Correlation of residual erosion surtaces in the eastern Appalachian Highlands : Geological Society of America Bullatin, v. 35, p. 633-668. Discusses drainage evolution, various erosion cycles, and attempts to correlate erosion surfaces .

Knopf , E. B. , 1929, '11le physiography of Baltimore County, Maryland, in Baltimore County, Maryland : Baltimore, Maryland Geological Survey, p. 58- 96 . Discusses physiography , erosion surfaces and correlation thereof . Contains some profiles and 3-D maps .

Knox , A. s., 1969, Glacial age marsh, Lafayette Park , Washington, D.C. : SLience , v. 165, p. 795-797 . Organic sediments from terrace 15 m above modern Potomac . Plant microfossils and ice-rafted boulders indicated a much colder climate . C-14 age of > 45, 000 yr and palynological studies suggest an early Wisconsin age .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Koch , C. A. , 1974, Debris slirtes and related flood events in the 4-5 Au gust 1938 Webb Mountain cloudburst; Sorre past and present envi ronmental geon�rphic implications [M.S. thesis]: Knoxville, University of Tennessee , 112 p. Main contribution is to supplement Moneymaker's (1938 ) article on the Webb Mountain flood. Describes revegetation process .

Kochel, R. c. , 1976 , Morphology, origin, and structural control of seve ral blockfields and associated deposits, northern Berks County, Pennsylvania (River of Rocks, Devils Potato Patch, and Blue Rocks) [Abstract]: Geological Society of America Abstracts with Programs , v. 8, p. 486-487 . Describes several bc•Jlder fields , sugge£ts formed by basal-slip sclifluction. Formation of block fields is favored in anticlinal valleys . Blocks find relative ease calving into the anticlinal valleys rather than sliding down dip slopes into adjacent synclinal valleys of similar litholog}·.

Kochel, R. C., 1987, Holocene debris flows in central Virginia, in Costa , J. E. , and Wieczorek, G. F. , eds., Debris flows/avalanches: Process, recognition, and mitj gation : Geological Society of America Reviews in Engineering Geology, v. 7: Boulder, CO, Geolog!cal Society of America, p. 139-155. Descrites debris flows in Nelson County area.

KochP.l, R. C. , and Johnson , R. A. , 1984, Geomorphology and sedimentology of humd d-temperatc alluvial fans, central Virginia, in Koster, E. H. , and Steel, R. J. , eds., Sedimentology of gravels and conglomerates: Canad . Society of Petroleum Geol., p. 109-122. Describes morphology and sedimentology of alluvial fans on west flank of Blue Ridge , and east of the Blue Ridge in Nelson County . Recurrence interval of latter estimated at 3,000 to 6,000 years.

Kochel , R. c. , Ritter, D- F. , and Miller, J. , 1987, Role of tree dams in the construction of pseudo-terraces and variable geomorphic response to floods in Little River Valley, Virginia: Geology, v. 15, p. 718-721 . During the 1985 flood in Little River valley, large trees eroded and transported by th� floodwaters were braced and stacked against trees still standing on the floodplain. Lateral barriers or dams created from these transported trees allowed the channel to be locally aggraded above the level of the floodplain. These featufes might be mistaken for terraces after they become vegetat� and the trees bracing the gravels decay .

Kuehne , R. A. , and Bailey, R. M. , 1961, Strearr. capture and the distribution of the percid fish Etheostoma Sagitta, with geologic and taxonomic considerations : Copeia, v. 1, p. 1-8 . Cites geomorphic evidence that uppe r Collins Fork was once tributary to Little Richland Creek but has been diverted into the Kentucky system by headwater capture . This allowed fish dispersal from the CUmberland basin to the Kentucky system .

Kuhaida, A. J., Jr. , 1971 , Debris avalanchir.g as a natural hazard in the southern Appalachians: A case study of the Davis Creek watershed , Virginia [M.S. thesis]: Johnson City, TN, East Tennessee Stote University, 69 p. Estimated degree of damage using aerial photos. Also characterized the various hazards resulting from the slides.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Kummel, H. B. , 1893, Some rivers of Connecticut : Journal of Geology, v. 1, p. 371-393. A general review of the geomorphology of Connecticut as known at the time .

Kung , H. , 1985, Critical erosion areas in Knoxville and Knox County, Tennessee : Journal of Th� Tennessee Academy of science , v. €0, p. 105-109. Approximately 10% of the studied area can be classified as critical erosion area; 6% is due to intense farmdng activities, 3% to construction, and 1% to road right-of-ways .

Kung , H., 1986, Effects of carbonate lithological characteristics on meander valley form [Abstract ): Geological Society of America Abstracts with Programs, v. 18, p. 250. Thirty stream-valley segments were studied in 12 different types of lithologic units. Asymmetrical valley form tends to occur in rocks wh ich have thick bedding and a high percentage of siliceous material , while symmetrical valley forms are favored in relatively pure 1 L.estone with few impurities and thin bedding.

Kung , H. , 1986, Relationship of rock solubility and drair.age density [Abstract ]: Geological Society of America Abstracts with Programs , v. 18 , p. 250 . Shows a Spearman's correlat1on of 0.88 between rock solubi lity cmd drainage density. In general , in the study area , high drainage density is associated with steep slopes, high elevations , and less-soluble rocks suet as shale; low density is on gentle slo�s , low elevation, and soluble carbonate rocks.

LaForge , L. L., Cooke, C. w. , Keith, A. , ar. J Campbell, M. R. , 1925, Physical geography of Georgia: Georgia Geological Survey Bulletin, v. 42, 189 p. Detailed description of the phys iography of Georgia .

LaMoreaux , P. E., and Madison, D. 0. , Jr., 1984 , The occurrence of sinkholes in the vicinity of the Southern Natural Gas Company Dry Valley pipeline , Shelby County, Alabama , in Nielsen, D. M., and CUrl, M. , eds. , Surface and borehole geophysical ruethods in ground �rater investigations , NWWJVEPA Conference , San Anton1o, TX, Feb. 7-9 , '84: Worthington , Oh io, Nat. Water We ll Asso. , p. 259-272 . Selected route for pipeline through karst atea using surface geologic mapping, photo interpretation, seismic refraction, and test drilling .

LaMoreaux , P. E., and Newton , J. G. , 1986, catastrophic subsidence : An envi ronmental hazard, Shelby County , Alabama: Environmental Geology and water Sciences, v. 8, �· 25-39 . Induced sinkholes commonly result from a water level decline due to pumpage . Construction activities in a cone of depression greatly increases the likelihood of sinkhole occurren.::e. Al100st all occur where cavities develop in unconsolidated deposits ove rlying solution openings in carbonate rocks. Shape , depth, and timing of catastrophic subsidence can be predicted in gene ral terms . Re100te sensing techniques are useful in predicting locations of such subsidence . Discusses activities likely to trigger catastrophic subsidence .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Lane , C. F. , 1951, Physiography of the Grassy Cove di strict , Cumberland County, Tennessee [Ph.D. thesis) : Evanston, IL, Northwestern Unive rsity, 165 p. Describes physiography of Grassy Cove .

Lane , C. F., 1952, Grassy Cove , a uvala in the Cumberland Plateau, Tennessee : The Tennessee Academy of Science Journal , v. 27, p. 291-295. A shortened section of the author's thesis.

Lane , C. F., 1957, Headward growth of anticlinal valleys in the karst cycle of erosion: Virginia Journal of Science, v. 8, p. 203-209 . The various stages in the karst cycle of erosion are illustrated in the separate coves as well as the processes that. were active during different stages of development . By studying the various phases of erosion in the several coves, the steps in the future headward growth of Sequatchie Valley can be determined.

Lane , C. F. , 1983, Physiographic provinces of Virginia: Virginia Geographer, v. 15, p. 25-29. Provides very brief descriptions of the physiographic provinces of Virginia.

Lattman, L. H. , 1953, Geomorphology of the Allegheny Mountain5 of east-central We st Virginia [Ph.D. thesis) : Cincinnati , University of Cincinnati , 152 p. Examines various aspects of the geomorphic evolution of the Allegheny Mountains .

Lattman, L. H. , 1954, The one-sided development of tributaries in tilted sedimentary rocks in the eastern Allegheny Plateau of west Virginia: Papers of th� Michigan Academy of Science , Arts, and Letters, v. 39 , p. 361-365. Finds support for hypothesis that tributaries are better developed on the up-dip side if the more resistant rocks crop out high in the section and on the down-dip side if the relatively resistant rocks are low in the section .

Lattman, L. H., 1960, Cross section of a flood plain in a moist region of moderate relief: Journal of Sedimentary Petrology, v. 30, p. 275-282. Reports on the cross section of a small floodplain in the Appalachian Plateau as seen in excavations and borings. Colluvium comprises almost one fifth of the total valley fill and contains isolated lenses of ve rtical accretion. Has generalized cross section.

Lattman , L. H. , and Nickelsen, R, P. , 1958 , Photographic fracture-trace mapping in the Appalachian Plateau : American Association of Petroleum Geologists Bulletin, v. 42, p. 2238-2245. Ma�� lineaments on aerial photos . Concludes that there appears to be a significant parallelism between the di rections of photogeologic fracture traces and bedrock joints .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Laurence , R. A. , 1937, Sinkholes of the Cumberland Plateau : Journal of Geology, v. 45, p. 214-215. Briefly describes sinkholes formed by collapse of very thick ov, •lying rocks into a cavern in the Bangor Limestone . Solution by q£ound water in the Bangor beneath the Plateau has evidently been very effective .

LaVal le, P. , 1967 , Some aspects of linear karst depressions in south central Kentucky: Association of American Geographers Annals, v. 57 , p. 49-71 . The percentage of structurally aligned depressions was found to be highest where limestones were characterized by low insoluble residue contents, where hydraulic gradients were high, where a high proportion of the surface runoff was concentrated in the subterranean drainage systems , and in areas wh ich were located near the oouth of the subte rranean drainage system.

LaValle, P. , 1968, Karst depression oorphology in South Central Kentucky: Geografiska Annaler, v. SO, p. 94-108. Mean depression area , relief, and flank slope inclination had high values where the following conditions prevailed: limestones were characterized by low mean i�zoluble residue contents, hyd raulic gradients were high, where a large percentage of the sur face runoff is diverted underground , wher� a high percentage of karst depressions were adjusted to lil�es of structural weakness, where dense limestones were encountered and in areas near the mouth of the karst drainage system.

LeGrand, H. , Stringfield, v. T. , and LaMoreat� , P. E. , 1976, Hydrologic features of United States karst regions , in Yevjevich, v. , ed ., Proceedings of the U.S. -Yugoslavia Symposium, Dubrovr.ik , J�e 2-7 , 1975: �t . �ollins , CO, Water Resources Publications, p. 31-46 . Briefly outlines hydrologic characterLr.ics of Ap�lachian provinces , alllOng others.

LeGrand, H. E., 1949, Sheet structure , a major factor in the occurrence of ground wate r in the granites of Georgia: Economi c Geology , v. 44, p. 110- 118. Imperfect shallow pseudosynclinal basins formed by sheet planes in valleys are the receptacles for much subsurface wat£r that percolates along these planes from nearby upland slopes.

LeGrand , H. E. , 1952, Solution depressions in diorite in North Carolina : American J�rnal of Science , v. 250, p. 566-585. Observed more than 40 enclosed depressions , ave raging about 200 ft in diameter and �t 3 feet in depth below the lowest possible ove rflow point . They are restricted to upland areas of dioritic rocks.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 LeGrand, H. E. , 1954, Geology and ground water in the Statesville area, North Carolina : North Carolina Department of Conservation and Development, Division of Mineral Re sources, v. 68, 68 p. Well yield is related to topographic location. The average yield of wells on hills is about half that of wells in othe r topo graphic locations and several times less than that of wells in draws . Seve ral tables show the relation of yield to type of r�ck , topographic location , and depth of well .

LeGrand, H. E. , 1967, Ground water of the Piedmont and Blue Ridge provinces in the southeastern states: U.S. Geological Survey Circular, v. 53� , 11 p. Well yields are greater in lowlands and draws and whe re a thick mantle of soil exists. Rocks underlying darker soils tend to yield water that is hard and contains objectionable amounts of iron, in comparison to rocks under light-colored soil . Where the water table is only a few feet beneath the land surface on an upland area, the rock fractures may be so scarce that water may not be able to move downward in the rock .

LeGrand , H. E. , 1973, Hydrological and ecological problems of karst regions : Science , v. 179, p. 859-864. Distinctive features of many karst terranes include scarcity of soils, scarcity of surface streams , �nd rugged topography ; less distinctive are the highly permeable and cavernous rocks, especially at shallow depths . High permeability gives rise to many practical problems , including scarcity and poor predictability of groundwater suppl ies, scarcity of surface streams , instability of the ground , leakage of surface reservoirs, and an unreliable waste-disposal environment . Appalachians are mentioned only briefly.

LeGrand, H. E., and Stringfield , v. T. , 1971 , Differential erosion of carbonate rock terraces: Southeastern Geology, v. 13, p. 1-17. Erosion in carbonate terranes is more rapid unde r moderate rather than under extreme conditions of cover, purity of the carbonate rock , topographic relief, a1d precipitation. Denuded carbonate rocks are much more resistant to physical and chemical erosion than are carbonate rocks with a moderately thin soil and vegetal cover ; where the soil and rock cover is very thick , physical erosion of the covered bed is impossible and chemical erosion may be retarded because of retarded water circulation. Briefly mentions Appalachians .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 LeGrand, H. E., and Stringfield, v. T , 1973, Concepts of karst development in relation to interpretation of surface runoff: Journal of Researcr �f the u.s. Geological survey, v. 1, p. 351-360 . The uneven distribution of permeabi lity beneath surface karst streams causes them to lose or gain water, depending on the position of the water table with reference to stream level . The conventional techniques of interpolation and extrapolation that have been reasonably successful in approxi�ting streamflow of ungaged sites in nonkarstic regions have only limi ted use in karst regions . An understanding of principles of karstification and an unde rstanding of the hydrogeologic framework of a carbo1.ate terrane provide a useful basis for evaluating the st:eamflow characteristics.

Leighton, M. 0. , 1904, Quality of water in the Susquehanna Rive r drainage basin, with an introductory chapter on physiographic features by CY. Hollister: u.s. Geological Survey water-Supply Paper, v. 108 , 76 p. Pages 9-18 briefly discuss the physiography of the basin area.

Leo, G. W. , Pavich, M. J., and Obermeier, s. F. , 1977, Mineralogical , ch�mical , and physical properties of the regolith ove rlying crystalline rocks , Fairfax County, Virginia: A preliminary report: u.s. Geological Survey Open-file Report, v. 77-644, 13 p. Purpose was to correlate variations in chemistry, mineralogy, and texture with engineering properties throughout the weathering profile. Coring sites were chosen to obtain a maximum depth of weathering on diverse lithologi'!!s. Analyses done of petrography, texture, clay-mineralogy, and major element chemistry. Shear strength and compressibility were also determined.

Leopold, L. B., 1973 , River channel change with time: An example: Geological Society of America Bulletin, v. 84, p. 1845-1860. Studied Watts branch near Rockville, Ma�yland. For the initial twelve years, the channel progressively but slowly became smaller as urbanization of the basin gradually proceeded. In 1966 ,

a threshold of change apparently was passed, and , probably as a result of an increased rate of land alteration upstream, large amounts of sediment were deposited in the channel and overbank . The number of floods exceeding channel capacity increased from an average of 2/Yr to more than 10/Yr . Urbanization did not alter the rate of channel migration.

Lesley, J. P. , 1869, Manual of coal and its topography: PhL<:odelphi ::�, J.P. Lippincott and Co ., 215 p. Include s one of the earliest discussions of how lithology and structure control topography in the Appalachians .

Lesley, J. P. , 1883, Gener�l introduction to Report D-3, in Second Geological Survey of Pennsylvania: Ha rrisburg, PA , Board of Conm . for the Geol . Survy, p. 27 . First to notice and describe the flat hilltop surfaces in the

valleys of the Valley & Ridge province .••"when looked down upon from the mountain, [it] appears like a great plain, which it really is."

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Lesley, J, P. , 1892 , Summary description of the geology of Pennsylvania, in three volumes: Ha rrisburg, PA , Board of Comm. for the Geol . Surv . Numerous references to topography and geomorphology. p. 685- 699 : elementary explanation of effect of structure on topography . In v. 3, p. 425 discusses caverns and sinkholes; p. 430, the rate of erosion; p. 433, the precipitation of limonite in caves .

Lessing, P. , 1979, Karst subsidence and linear features , Greenbrier and 11onroe counties, West Vi rginia [map] : West Virgin'a Envi ronmental Geology Bulletin, v. EGB-17, 1 p. Map, scale 1:50,000, shows areas that have experienced sinkhole collapse in red ; lines are drawn through linear concentrations of sinkholes, though individual sinkholes are not shown .

Lessing, P. , and Erwin , R. B., 1977 , Landslides in We st Virginia, in Coates, D. R. , ed. , Landsl ides: Geological Society of America Reviews in Engineering Geology: Boulder, CO, Geological Society of America, p. 245-254 . Di�cusses la�dslides and mapping program. Slides correlate well with the orcu�: �nee of red shale bedrock , slopes of 15% to 45% . concave topographic slopes, and certain actions of man .

Lessing, P., Kulander , B. R. , Wilson, B. D. , Dean, s. L. , and Woodring, S. M. , 1976, West Virgini a landslides and slide-prone areas: West Virginia Environmental Geology Bulletin, v. 15, 64 p. Rather popular discussion of landslides and the ir c�uses. Accompanying �1e report are landslide mars of 28 quadrangles, showing recent landslides, older landslides, rockfalls, slide-prone areas, and relatively stable ground .

Lessing, P. , Missina, C. P. , and Fonner, R. F., 1983, Landslide risk assessment : Env ironmental Geology, v. 5, p. 93-99 . Authors randomly selected 2,416 landslides from 31 mapped quadrangles. For each landslide , 12 geological factors were tabulated and coded : formation name; dip direction and angle; systematic fracture direction; us� soils series; slope percent; whether slide was parallel , perpendicular, or equidimensional to slope; landslide azimuth; landslide area; old or new slide; whether slide was associated wi th mine spoil; whether top:>graphy was concave , convex , planar, or complex ; and numbe r of slides within 1,000 feet. From the results of this analysis, the vulnerability of a given location to sliding can be statistically evaluated. Found that 60 percent of slides have concave topography , slides have have no preferred di rection, and dip slopes do not favor slides.

Leverett , F. , 1897, Changes in drainage in southern Ohio: Deni son Univers.ity Bul J.etin, Journal of Scientific Laboratory, v. 9, p. 18-21. Discusses an abandoned valley that is a continuation of the old Kanawha system. It departs from the present Ohio at Wheelersburg, ohio, about 10 miles above Portsmouth, and passes northward in a somewhat winding course to the Scioto River opposite the city of Waverly.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Leve rett , F. , 1902, Glacial formations and drainage features of the Erie and Ohio basins : u.s. Geological Survey Monograph, v. 41, 802 p. On p. 100-109, discusses the old Kanawha drainage system in southern Ohio.

Leverett, F. , 1929, The Pleistocene of northern Kentucky: Kentucky Geological survey series VI, v. 6, p. 1-80. Excellent discussion of many aspects of Pleistocene geology in Kentucky. Includes sections on residuals on uplands , Tertiary deposits, Early Pleistocene fluvial plains, drainage peculiarities, pre-Illinoian glaciation, drainage evolution, loess and wind-deposited deposits.

Leverett, F. , 1934 , Glacial deposits outside the Wisconsin terminal moraine in Pennsylvania: Pennsylvania Topographic and Geologic Survey 4th Series Bulletin, v. G7 , 123 p. Di scusses glacial deposits and landscape changes in pre�isconsin time .

Leverett, F. , 1939, Stream capture ar.d drainage shifting in the Upper Oh io region: Journal of Geomor��ology, v. 1, p. 339-344. Outlines the major shifts in dra1nage in that part of the Oh io Valley bordering the W�st Virginia Panhandle. Two distinct systems of drainage had been developed, the southern one more than 100 ft lower than the northern. This conditior. was highly favorable for stream capture and progressive encroachment by the southern drainage system of territory that had been held by the northern .

Lewis, L. A. , 1968, Analysis of surficial landform properties - the regionalization of Indiana into units of morphometric similarity: Indiana Academy of Sciences, v. 78, p. 317-328. Used various morphometric measures on randomly selected topo maps to develop regional geomorphic units for Indiana . Says previous physiographic units fail in del iminating the state into regions of foil" similarity.

Lewi s, S. E. , 1975, Geology of the southern part of the Riner Quadr. Jle, Montgomery and Floyd counties , Virginia [M.S. thesis]: Raleigh, NC , North Carolina State university. Mapped and discussed terraces along the Little River (tributary to New River ).

Lewis, s. E. , and Bartholomew, M. J., 1976, Cenozoic structural control and evolution of the Little River drainage system in the Blue Ridge/Valley and Ridge provinces, southwestern Virginia [Abstract ]: Geological Society of America Abstracts with Programs , v. 8, p. ::'.1.9-220. Terrace development indicates that incision of �e Little River took place in three stages. The oldest terraces (30 m above present floodplain) do not closely reflect the present-day distribution of channels as indicated by an abandoned 3 km segme�t of Brush Creek, a tributary. Development of pre�P.nt-day drainage pattern was achieved during formation of internv . ate-level terraces (25 m) . Youngest terraces occur betw< _n 7-12 m. Patterns r�flect Paleozoic structural trends .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Liebling, R. S. , and Scherp, H. s., 1984, Development of the Susquehanna River drainage across the folded Appalachians : Northeastern Geology, v. 6, p. 1- 3. Concludes that the course of the Susquehanna River drainage across the ridges follows a focal line of lowest elevation on a former baselevel wh ich presently is represented by ridge crest elevations ranging from 1300-1500 ft. According to this reconstruction, the channel position on this paleo-erosional surface was pre-detet�n· i by the structurally-controlled distribution of highland areas of resistant bedrock located to the east and west. With regional upl ift of this former baselevel, these highlands continued to delineate an essentially N-S oriented drainage basin.

Liebling, R. S. , and Scherp, H. s. , 1984, Stream pi racy at the base of th� Allegheny Front, central Pennsylvania: Northeastern Geology, v. 6, p. 131- 134. The pronounced , northeast-trending valley along the base of the Allegheny Plateau is dominated by the northeast-flowing Bald Eagle Creek-west Branch Susquehanna River system. The southwestern part of the valley, however, is ocl�pied by 3 separate drainage basins. Each containo paired headwater tributaries which flow more or less parallel to the strike of the valley but which discharge L, eir wa�ers to the southeast across the trend of the structures. Authors argue that Bald Eagle Creek once extended the enti re length of the valley and was later subjected to a series of stream captures occurring sequentially from southwest to northeast.

Lintner, S. F., 1983, The historical physical behavior of the Lower Susquehanna River, Pennsylvania (1801-1976 ) [Ph.D. thesis]: Baltimore, Johns Hopk ins University, 208 p. Describes and analyzes a 12.5-km reach of the river in Lancaster County. Develops a river chr�nology which relates physical change in the study area to channel processes reflecting regional land use changes . 'Ihe oost important change has been storage of anthracite coal waste in the river. Sediment yields have declined since 1956 .

Lebeck, A. K. , 1929, The geology and physiography of the Mallatloth Cave National Park : Kentucky Geological Survey Series VI, v. 31 , p. 327-399 . General discussion of the physiography of the Mammoth Cave area .

Lorenz , P. J. , 1972, The sandstone sinkholes of the Cumberlands [Abstract ] : Tennessee Academy of Science Journal , v. 47, p. 57. Twelve large sinkholes on the CUmberland Plateau in or near Grundy County, Tennessee , were investigated. All were in the Crab Orchard Formation (Sewanee Conglomerate ) and were fo��d to be located within a few hundred feet of the escarpment.

Losche, C. K. , 1967, Soil genesis and forest growth on steeply sloping landscapes of the southern Appalachians [Ph.D. thesis]: Raleigh, NC , North Carolina State University, 194 p. St• ·died depth of rooting, clay and clay mineralogy, organic matter, �xtractable iron, numus , particle size of soils on steep hillslopes . Particularly compared north and south aspects.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Lucke , J. B., 1941, Gravel indications of New Jersey drainage changes: Journal of GeOJOOrpi.ology, v. 4, p. 265-284. In a limited area on the Fall Zone near New B�swi ck occur bedded gravels of such a character that they are regarded as 1) definitely fluvial ; 2) essentially in place ; 3) depwsition products of a major stream draining a region outside New Jersey.

Luft, S. J., 1986 , The South Fork of the Licking River - eastern Kentucky 's major late Te rtiary river?: Southeastern Geology, v. 26, p. 239-249 . Five lines of evidence suggest that in preglacial late Te rtiary time, the South Fork was a much longer stream, drained a larger area, and may llave be'i!n the trunk stream of the Licking River system: 1) present stream is underfit; 2) qua rtz and chert clasts whose bedrock source is well beyond the present drainage area are abundant in Tertiary gravels of the stream; 3) a wide , well-defined valley of intermediate altitude apparently headed far beyond present drainage divides; 4) wavelengths of Teay-age valley are out of proportion to the present drainage area; and 5) gP.omorphic characteristics of the Kentucky River gorge suggest it was the channel '::Jy which the South Fork was captured by the Kentucky River.

Lund , S. P., 1981 , Late Quaterna.y secular variation of the earL�'s magnetic field as recorded in the wet sediments o� three North America."l lakes [Ph.D. thesi�]: Minneapolis, university of Minnesvt3 , 300 p. Attributed changes in magnetic-field intP.nsities ove r time in Ande rson Pond cores to changing contents of magnetite, which in turn results from �hanging source areas supplying sediment to the pond . More distant sources seemed to be supplying the pond during glacial conditions . The pond is south of Cookeville, Tennessee .

Lu sk, R. G. , 1928, Gravel on the Highland Rim plateau and terraces in the valley of cumberland River: Journal of Geology, v. 36, p. 164-170. Two patches of gravel on the Highland Rim are interpreted as deposits of the old CUmberland River when it meandered on a plai� several hundred feet above the bottom of its present valley. PatcheG are 400 ft or more below the general level of the plateau.

Lutz, H. J., 1940, Disturbance of forest soil resulting from the uprooting of trees: Yale University School of Forestry Bulletin, v. 45, p. 1-37 . Dug trenches through mounds formed by tree throw, described properties of soil so disturbed with other soil. Found a number of physical and chemical differences. Figure 7 is a 1-ft contour-interval map showing microrelief in a 0.1-acre plot .

Lutz, H. J., and Griswold, F. S. , 1939, The influence �f tree roots on soil morphology: American Journal of Science , v. 237, p. 389-400 . Describes very irregular soil profiles in forests, which the authors attribute to the action of roots by tree throw, leaving root canals, pushing soil aside during growth , and agit3tion of soil as trees sway in strong wind .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Macar, P. , 1955, Appalachian and Arder�es levels of erosion compared : Journal of Geology, v. 63, p. 253-267 . Author recognizes up to 10 erosion levels in a vertical range of 250 m in Belgium, and saw quite similar surfaces in the Appalachians .

Mackin, J. H. , 1933, The evolction of the Hudson-Delaware-susqueharma drainage : American Journal of Science , v. 26, p. 319-331 . The marked parallelisms of the NE-SW flowing streams of the Atlantic slope wi th the trend of Appalachian structures suggests that they are either consequent on the initial surface of the folds , or subsequent on the banded outcrop of folded rocks of variable resistance . The relation of streams to the plunge of the structures which they follow indicates conclusively that they cannot have bf>�n consequent upon them.

Macki1�. J. H. , 1934, Terraces in the Susquehanna Valley below Harrisburg, Pennsylvania: Science , v. 80, p. 140-141 . The terrace stands 90-110 ft above the river at nearly the same elevation as broad lowlands of the well-known Somerville peneplane . The presence of rock types foreign to the drainage basin of the Susquehanna in the Somerville terrace gravels indicates that the Somerville cycle was interrupted du ring or after t..'te advance o! some ice sheet; the author thus fixed the age of the Somerville peneplain as Pleistocene .

Mackin, J. H. , 1938, The origin of Appalachian drainage - a reply: American Journal of Science , v. 236, p. 27-53 . Attacks Meyerhoff and Olmsted's � 936 paper. Cites problems with their theory, says it will not serve to replace the Johnsonian concept of regional supe rposition of Appalachian streams from a Cretaceous cover.

Mackin, J. H. , 1941, Drainage changes near Wind Gap, Pennsylvania - a study in map interpretation: Journal of Geomorphology, v. 4, p. 24-52. The possibility that the Wind Gap River might have been diverted by early Pleistocene glaciers, rather than by normal capture, must be recognized, for the date of the diversion, whether Pliocene or Pleistocene , is uncertain.

Malott, c. A. , 1920, Static rejuvenation: Science , v. 52, p. 182-183 . When the present Ohio invaded the basin of the much smaller pre-glacial stream the local peneplain was statically rejuvenated , due to the sinking of the larger stream into the plain on account of its ability to possess a much l��r gradient in its grade condition.

Malott, C. A. , and Shrock ,. R. R. , 1930, Origin and development of Natural Bridge , Vi. rginia: American Journal of Science , v. 219, p. 257-273 . Attributes formation of the bridge to subterran�an diversion. Figures 2-5 show hypothesized development of subte rranean cutoff.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Maness, L. V. , Jr., 1977 , A quantitativ� geomorphic study of stream valley syrrmetry in the Bluegrass region of Northern Kentucky [M.S. thesis]: Terre Haute , IN, Indiana State university, 122 p. Found that distance from former tenmini of continental olJciers, joints, stream order, lithology, and climate alJ significantiy affected stream-valley symmetry. 80 percent of valleys are asymmetrical in this region .

Mann , R. A. , 1982, cave development along selecteci areas of the western Cumberland Plateau escarpment [M.Sc. thesis] : Memphis, Memphis State university, 91 p. Applies and modifies Crawford's theory of cave development along the Cumberland Plateau escarpment . Says Crawford 's theory doesn 't explain many phreatic features in caves. Has cave maps supe rimposed on topo maps.

Marchand , D. E., 1978 , Quaternary deposits and Quaternary history of central Penn,:;ylvania: Pennsylvania State university Agronomy Oepartlllent , Agronomy Series no. 52, v. 52 , p. 1-19. A brief account of the glacial history of central Pennsylvania; in Marchand , D. E., and others, Quaternary deposits ana soils of the central Susquehanna valley of Pennsyl •ania, 89 p.

Marchand, D. E. , Ci"lkosz , E. J. , Bucek , 1-1 . F. , and Cre��o:l, G. H. , 1978 , Quaternary positsde and soils of the central Susquehanna valley of Pennsylvania: Pennsylvania State university Agronou¥ Department , Ag ronomy Series, v. 52, 89 p. See individual articles

Marland , F. C. , 1967, The history of Mountain Lake, Giles County , Virginia : An introduction based on paleolimnology [Ph.D. thesis ]: Blacksbu:g, VA, Virginia Polytechnic Institute , 129 p. Took cores of bottom se

Marsh, B. , 1987, Pleistocene pingo scars in Pennsylvania : Geology, v. 15, p. 945-947 . Pleistocene open-system pingo scars identified in Va lley and Ridge of central Pennsylvania . The features are ellipti :al basins averaging 20 by 50 m in plan and 4 m in depth, bounded by low ramparts . Located beyond the limits of Pleistocene glaciation, they closely resemble features reported as pingo scars in England , and they are dated at 12.8 I

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Martin, R. A. , 197�, Gee!( · �, e Devil's Racecourse boulderfield , Dauphin County, Pennsylvania :act]: Ceological Society of America Abstracts with Programs, v. 4, , .).J-31. Describes chaL.:.c\..�dstics of the boulder fields . Notes that smaller and more rounded boulders are gene rally found below the surface , while largPr and more angular ones occur on the surface . The dish-shaped boulde rs are mostly steeply dipping (60-90 deg. ) and well oriented parallel to the length of the boulder streams . The long axes of the rod-shaped boulde rs are generally oriented parallel to the trend of the boulder field.

Matthews , L. E. , 1971, Descriptions of Tennessee Caves : Tennessee Division of Geology Bulletin, v. 69, 150 p. Supplements Barr's 1961 guidebook.

Matthews , L. E. , 1973, Hydrogeology of the CUmberland Escarpment, Tennessee : Speleonews , v. 17, p. 92-96 . The escarpment contair.s 2 perched water tables and 1 normal water table. �e upper perched water table is developed within the capping Pennsylvanian rocks and is on top of the Pennington shales. The lower perched water table is within the base of the Bangor Limestone and is on top of the shaly Hartselle Formation. The normal water table is developed in the Monteagle Limestone . Its position is determined by the base level of the local stream. The position of the normal water table gradually lowers through time as the local streams continue to downcut .

Matthews , w. H. , 1975, Cenozoic erosion and erosion surfaces of eastern North America: American Journal of Science, v. 275, p. 818-824 . Used volume of Cenozoic deposits in the western Atlantic Ocean to derive a Cenozoic erosion rate for the source area (assuming the western limit of the latter to have persisted near the present crest of the Appalachian Mountains ) of about 2 kn of denudation in 65 m.y.

May, J. P. , 1966 , Stream valley geometry as an index to the evolution of the Piedmont surface [M.S. the sis] : Chapel Hi ll , NC , University of North carol ina , 61 p. Classified stream valleys into , �·ttin9, graded , and compound. Compound represents a reve rsio. �rom graded to downcutting �d consists of a graded head , a zone of incision, and a regraded zone . This type valley results from a lowering of base level and causes a

zone of incision to progress from mouth to head ••..zones of incision and valley "shoulde rs" occur independent of rock type and structure . Othe r topographic forms and drainage trends are not ubiquitously controlled by bedrock character. These geometric relationships support the theory that the Piedmont surface of North Carol ina represents an upli fted and dissected peneplain.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mayer, L. , and wentworth, c. M. , 1983, Geomorphic differences east and west of the Stafford fault system, northeastern Virginia [Abstract): Geological Society of America Abstracts with Programs, v. 15, p. 56 . Preliminary topographic analysis of small drainage basins indi cates that stream gradients west of the Stafford fault zone (SFZ ) are consistently steeper than those east of it, in �J th Piedmont and Coastal Plain. Channels west of the SFZ tend to be more convex than those to the east . 82 % of the drainage basins were correctly classified as either east of the SFZ or west of the SFZ solely on the basis of a linear function of geomorphic parameters. Convexity is characteristic of stream channels that have experienced a base-level fall. Such a fall would be consistent with the sense of relative motion across the SFZ .

Mayfield, M. W. , 1979, Runoff in the Obed-Emory River basin of Tennessee : Southeastern Geographer, v. 19, p. 54-65. Streamflows show great short-term variability. Rapid subsurface transmission of water is favored by thin, highly permeable soil and by underlying bedrock o: low permeability �� t keeps th e water near the surface and greatly restricts access to the slow, indirect routes of deep outflow.

Mayfield, M. w. , !981 , Streamflow characteristics of the CUmbe rland Plateau, in Hill , R. T. , cd. , Conference on Appalachian Geography , Pipestem State Park, Pipestem, WV, Oct. �-3, 1981 : Proceedings : Athens, WV, Concord College , p. 1 !::-25. Th� �an annual floods of Plateau streams are much hig�er per unit area than other Tennessee streams. Author attributes thi s to low permeability of the Plateau �rock and the high permeability of thin soils, which allows rapid throughflow to the stre� channels. Base flows are correspondingly low. Streams with highest flood peaks drain areas exclusively underlain by conglomeratic bedrock .

Mayfield, M. w. , 1986, Response of the fluvial system to floods in the southern Appalachians, in Third Conference ?n Appalachian Geography : Pirestem State Park, Mar. 14-16, 1986 , Proce,:!dings: Athens, WV, Concord College , p. 82-85. Ring counts on more than 50 trees at gravelly point bars of the Obed River, Emory er,Riv Whites Cre'1k , and Clear Creek confirm that these deposits are not disturbed by floods wi th recurrence levels less than 15 years at the minimum. This findlng is particula.rly surprising in light of the fact that these st�eams produce unit-area floods some 100-200 percent gr�ater than r�gional ave rages. Study area was Cumberland Plateau, Tennessee.

Maynard, �. R. , and Humbertson, P. G. , 1975, Some jointing and stream pattern relationships in southwestern Pennsylvania [Abstract ): Geological Society of America Abstracts with Programs , v. 7, p. 93-94 . From 25 sites, a total of 412 joint strikes and 2,015 feet of exposed joints were measured. Multiple joint site measurements correspond with stream direction tendency better than individual site tests. Between 70-89 % of the tctal stream lengths correlated with exposed joint strikes occurring within the basin.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 McCampbell , J. C. , 19S2, Structural evidences for the presence of a wa rped peneplain unde r the North Carolina Coastal Plain [Abstract ): Geological society of America Bulletin, v. 63, p. 1277 . Either one considerably warped or two separate peneplains exist below the sed1ments. The surfaces cannot readily be correlated with current recognizable peneplains of the Blue Ridge and Valley and Ridge areas . Rather, there seems to be a warped single surface whose slope has been exaggerated by downwa rd adjustment due to compensation for the additional weight of the Coastal Plain sediments. It is believed that the adjustment took place during the whole period of deposition of the materials .

McCarten, L. , Gonzale=, V. M. , and Bugen, M. , 1985, Southern Maryland grave ls probable sources and history [Abstract]: Geological Society of hne rica Abstracts with Programs , v. 17, p. 122-123. Most clasts derived from Piedmont and Va lley and Ridge . About 50 percent of gravel probably derived from a P'oto-Susquehanna River, and remainder from a proto-Potomac, based on mineralogy of clasts. The mouth of the Potomac was about the same as it is now or slightly to the west during Miocene, early Pliocene , and Pleistocene , but was about 70 km farther east late in the Pliocene .

McCracken , R. J., Shanks, R. E. , and Clebsch, E. E. c. , 1962, Soil morphology and geneeis at highe r elevations of the Great Smoky Mountains: Soil Science Society of America Proceedings , v. 26, p. 384-388. sc ,.ls placed into two groups : 1) those lacking A2 horizons with thin A1 and "color" B ho rizons , and 2) those with A2 horizons , Bi r horizons, and relatively thick mor layers. Soils of 1) occupy well drained sites unde r spruce-fir forest, and those of 2) occupy less well nrained sites under heath bald or rhododendron unde rstory of spruce fir, with some indication tha1: they tend to form from more quartzose conglomeratic rock .

McGee , w. J. , 1888, The geology ol the head of Chesapeak� say : u.s. Geological Survey Annual Report, v. 7, p. 537-646. Describes geology and ysiogph raphy of Piedlnc:- j Coastal Plain.

McGee, w. J. , 1888, Three formations of the middle Atlandc slope : American Journal of Science , v. 35, p. 120-143, 328-330, 367-388, 448-466 . Three formations refer to those of th e Coastal Plain. However, author dwells on the Piedmont, also. Recognized "base-level " plains on the Piedmont . McGee was one of the pioneers in emphasizing how much a consideration of geomorphic forms could aid the study of geologic history.

McGee, w. J. , 1896, Geographic hi�tory of the Piedmont Plateau ; National Geographic Magazine, v. 7, p. 261-265. Popular account , stressing that uplift of the Piedmont is ongoing.

McGrain, P. , 1954, Geology of the Carter and Cascade caves area: Kentucky Geological �urvey, Series 10, Special Pub . 12, 32 p. Popular account of geology and geomorphology of the area , stressinc caves.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 McGrain, P. , 1955, GP.ology of the Cumbe rland Falls State Park area: Kentucky Geological Survey , Series 10, Special Pub . 11 , 33 p. Popular account of geology, phy�icgraphy, effect of bedrock on geomorphology , and probable history of some geomorphi c features,

McGrain, P. , 1962, Geology of Mammoth Cave National Park arEa: Kentuc

Geological Survey, Series 10, Special Pub . 7, 40 p. Popular guide to geology of Mammoth Cave ; now supplanted by Palmer (1981 )

McGrain, P. , 1976, Lapies-type features in the Kentucky karst region: Highway Geology Symposium Proceedings , v. 27 , p. 132-137. Describes examples of lapies-like solution features in the Kentucky karst region.

McGrain, P., 1979, Recognition of lapies-type features in the Kentucky karst an example of applied geomorphology: Kentucky Academy of Sciences Transactions, v. 40, p. 21-26 . Describes examples of lapies-like features, and points out importance of understanding the occurrence and distribution of irregularly dissolved uppe r surfaces of limestone strata .

Mcvrain, P. , and CUrrens, J. C. , 1978, T�pography of Kentucky: Kentucky

Geological Survey, Series 10, Special Pub . 25, 76 p. Describes topography county-by-county, occasionally throwing in a little geomorphology.

McKeon , J. B., 1974, North Carolina glacier: Evidence disputed: Science , v. 184, p. 88-91 . Disputes evidence of Berkland and Raymond (1973 ) for Pleistocene glaciation on Grandfather Mountain.

McMaster, W. M. , and Hubbard , E. F. , 1970, Water resources of the Great Smoky Mountains National Park, '.L'ennessee and North Carolina [maps) : U.S. Geological Survey Hydrological Investigations Atlas, v. HA- 420, 2 p. Sheet 2 is groundwatP.r availability map, which reflects surface deposits. Low favorabil1ty indicates ridge location, moderate favorability indicates minor valley location, and high favorability indicates major valley location . Representative yields and water chemistry are given.

McSaveney, E. R. , and Kaye , J. M. , 1974 , Compositional sorting of topographically high Tennessee River gravels: A glacial hypothesis [discussion and reply): Geology, v. �. p. 281-282 . Mc5aveney attack 's Kaye 's (1973) hypothesis of former glaciation in the Blue Ridge .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Meade , R. H., 1982 , Sources, sinks, and storage of river sediment in the

Atlantic drainage of the Un ited States: Journal of Geology, v. 90, p. 235- 252. Soil erosion was accelerated at least lOX by agriculture . Al though rates of erosion of cropland have been reduced , large quantities of eroded material are still stored on hillslopes and stream valleys where they continue to augment the sediment load of rivers. This sediment can be expected to emerge from storage for many decades and perhaps centuries to come . Reservoirs trap significant portions of the moving sediment. Essenti.ally all the river sediment that reaches the Atlantic coastal zone is trap� in estuaries and coastal marshlands . Probably less than 5 \ is deposited on the continental shelf or the deep sea .

Meade , R. H., and Trimble, S. w. , 1974, Changes in sediment loads in rivers of the Atlantic drainage of the United States since 1900, in Effects of man on the interface of the hydrological cycle with the physical environment - IAHS-AISH Publ . no. 113: Paris, IAHS-AISH, p. 99-104 . Sediment loads have decreased immediately downstream from reservoirs but the persistence of large loads at points farther downstream indicates that the river channels themselves are now being degraded. The decline of crop farming and the improvement of soil-conservation practices has also decreased the sediment yields, but this is r£'flected mainly in the sediment loads of the tributary streams; as yet, there has been no correspondingly marked decrease in the sediment loads in most of the main-stem rivers. Add to reference : Proceedings of the Paris Symposium, September 1974 .

Medville, D. , and Werner, E. , 1977, Karst hydrology and water chemistry in a mixed sedimenta�{ terrain, in Tolson , J. s. , and Doyle, F. L. , eds. , Karst hydrogeology: Memoirs of the 12th Congress of the International Association of Hydrologists, u. Alabama - Hun�sville: Huntsville, AL, Internat . Asso. Hydrogeologists, p. 443-457. Only 5-10 \ of surface is carbonate . Surface streams are captured at the upper contact of the limestones and numerous springs occur at contacts of carboP4 te and non-carbonate beds . Local variations of geology are far more significant in determining water chemistry than structural or stratigraphic variations of regional scale.

Medvi lle, D. M., and Storage , w. K. , 1986, Structural and stratigraphical influences on the development of solution conduits in the uppe r Elk Riv� r Valley, ��st Virginia: NSS Bulletin, v. 48, p. 8-25. Discusses the nature of the underground flow paths of the Elk River and •ts tributary, outlines a sequence of cave development for L� e area, an� relates the caves to structural and stratigraphic influences.

Meentemeyer, V. , and Zippin, J., 1980, Observations of needle ice growth and potential (•,r accelerated erosion on the Georgia Piedmont : Southeastern Geographer, v. 20, p. 31-41. Reports field studies on tne microclimatic and soil conditions under which needle ice will grow on the Georgia Piedmont . Concludes that the contribution of needle ice to erosion in th� Piedmont is very important, particularly on bare soil.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Meijer, w. , Campbell, J. J. N. , Setser, H., and Meade , L. E. , 1981 , Swamp forests on high tarrace deposits in the Bluegrass and Knobs region of Kentucky: Castanea , �. 46 , p. 122-135. The distribution of swamp forest sites as indicated by Quercus bicolor was mapped. Most of these are on high level terraces probably deposited by rivers ponded during glaciation.

Me isler, H. , 1962, Origin of erosional surfaces in the Lebanon Valley, Pennsylvania: Geological Sc _ ty of America Bulletin, v. 73, p. 1071-1082. Postulates that stream capture and normal erosion of differing rock types have produced the present landscape features in relatively recent time and that this was accomplished without appreciable change of regional base level . Notes that although accordant summits occur ove r large areas, summJts are not accordant between adjacent areas within the valley. Shows topographic profiles, h�psometric curves, and drainage evolution maps .

Melhorn, W. N. , and Edgar, D. E., 1975, The case for episodic continental erosion surfaces: A tentative geodynamic model, in Melhorn, w. N. , and Flemal, R. C. , eds. , Theories of landform development : Binghamton , NY, s. U.N.Y. - Binghamton, p. 243-276 . Authors provide correlation table that includes Appalachian erosion surfaces. Suggest worldwide correlations exist and attempt to provide a basis for this correlation, drawing upon geotectonic studies of the scope and periodicity of crustal toovement and deformation through time .

Menard, H. W. , 1961.- Some rates of regional er')sion: Journal 'lf Geology, v. 69 , p. 154-161 . Calculates past and pre�ent erosion rates for Appalachian region, atoong others. The ave rage rate of erosion of this region during the last 125 million years (determ. from onshore and offshore sediment wedge ) is 7.8 times as fast as at present (from river sediment loads ): 62 mmv1000 yr vs . 8 mm/1000 yr.

Merril, G. K. , 1960, Additional notes on vertical shafts in limestone caves: NSS Bulletin, v. 22, p. 101-108. The general form of domepits is a result of the highly uniform characteristics of the limestone bedrock and a zone of concentrated water seepage either in a sinkhole or along ridge margins. Usually they are formed where ravines intersect the ridge . The domepits frequently occur in series, developing along with headward valley erosion.

Meyerhoff, H. A. , 1940, Migration of erosional surfaces: Association of American Geographers Annals, v. 30, p. 247-254. Entrenchment proceeds in a leisurely fashion from stream toouth to stream source , with each successive set of cyclical forms migrating progressively upstream. upstr�� erosional forms wh ich have developed in Quaternary time were inaugurated by uplifts wh ich occurred near the stream toouths at a much earlier geological date . Also, however rapidly lateral planation by streams may broaden valley floors, the process of valley floor gradation is also carried on by sheetwash in the development of graded wash slopef .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Meye rhoff, H. A. , 1972, Postorogenic development of the Appalachians : Geological Society of America Bulletin, v. 83, p. 1709-1728. Structural , stratigraphic, lithologic, and topographic evid��ce collectively points to no substantive change in di�ection of stream flow since Permian time .

Meyerhoff, H. A. , 1975, The Penckian model - with mod1i\cations , in Melhorn, w. N. , and Flemal, R. C., eds. , Theories of landforn• development : Binghamton , NY, S.U.N.Y. - Binghamton, p. d5-68 . Field and map cu�lysis OI western New England's upland surface demonstrates the succession of erosional terraces or straths . The surfaces were formed by successive ve rtical changes in sea level, with progressive headward entrenchment of streams and partial cyclical development of valley floors. The concept, which is basically the Penck model , has worldwide application for fluvially dissected landforms .

Meye rhoff, H. A. , and Huabell , M. , 1928, The erosional landforms of eastern and central Vermont : Reports of the Vermont State Geologist, v. 1927-28, p. 315-381. Supports Barrell's conclusion that the New England upland is a te rraced upland . Thinks the terraces were formed during numerous cycles of erosion, at least 14 in numbe r. Lack of warping suggests New England has been raised in a series of vertical uplifts . Terraces are of fluvial origin, not marine .

Meyerhoff, H. A. , and Olmsted , E. w. , 1934 , Wind gaps and water gaps in Pennsylvania: American Journal of Science , v. 27, p. 410-416. Authors take issue with Ver Steeg's (1933) conclusion that wind gaps have no significance for erosional history. They examine Ve r Steeg's table of wind-gap elevations and claim to see groupings. By making the assumption that the lowest elevation in a group of gaps most n�arly approximates the local base of erosion, they find some correspondence with a chart of peneplain elevations compiled from several authors.

Meyerhoff, H. A. , and Olmsted, E. w. , 1936, The origins of Appalachian drainage : American Journal of Science , v. 232, p. 21-42. Several independent lines of evidence point to the Permo-Triassic origin of the main streams that drain the central and northern Appalachian region. The geographic distribution of Paleozoic stratigraphic units an i the nature of the fold- and fault-structures indicate that the original drainage divide was located west or northwest of the Great valley in Triassic time, and that its position was a direct result of the Appalachian orogeny .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mia, M. M. , 1978 , Effect of drainage basin size on channel and valley geometry: A case study of thi rd, fourth, and fifth order streams from the unglaciated Allegheny Plateau [Ph.D. thesis): Pittsburg, Un iversity of Pittsburg, 141 p. Measured channel and valley cross sections at 100 stations and

related these data to basin area. For all groups, r = .85 between

cross-sectional area arui basin size, with b • .61 in the regression equation. The r for width vs . basin size was .81. For width/depth

ratio, r • .02. Major residuals can be explained aJ availability of bedload, va riation in bed material, variation in bank material, and variation in slope .

Michalek, D. D., 1968, Fanlike fe�tures and related periglacial phenomena of the southern Blue Ridge [Ph.D. the�; s): Chapel Hill, NC , University of North Carolina, 198 p. Characterizes geographical &"1 elevational distribution and morphology of fans and block fields in the southern Blue Ridge , and provides a paleoclimatic interpretation . Fan apex elevation ranges in elevation from 2200 to 4000 ft, with the great majority above 2800 ft. Suggests mean annual temperature was decreased about 15 degrees F, that the snow line lowered to 6500 ft, and treeline to 3000-3500 ft. No fans observed SO\lth of Asheville, NC , and few along the Blue Ridge front.

Middlekauf , B. D., 1981, Wisconsinan biotic shifts in the central Appalachians, in Hill, R. T. , ed., Conference on Appalachian r� oqraphy, Pipestem State Park, Pipestem, WV, Oct. 2-3 , 1981 : Proceedings : Athens , WV, Concord College , p. 1-14. Discusses palynological and paleontological evidence for the existence of a rigorous late Wi�consinan paleoclimate in the Central Appalachians . Discussion of faunal evidence is particularly useful .

Milici , R. C., 1960 , The geology of the Sequatchie Va lley ove rthrust block , Sequatchie Valley, Tennessee [Ph.D. thesis): Knoxv] lle, TN, University of Tennessee, 83 p. On p. 15-16 author briefly discusses topographic expression of formations. Includes good 3-D physiographic sketch.

Milici, R. c. , 1965, The physiography of Sequatchie Valley and adjacent portions ot the Cumberland Plateau, Tennessee : Southeastern Geology, v. 8, p. 179- 193 . Applies dynamic equilibrium princip� cs to observations made in detailed geologic mapping of the area. Fig. 3 is an excellent 3-D sketch showing relationship of physiography to bedrock geology in the cencral Sequatchie Valley. Surficial deposits discussed include 3 terrace levels and alluvial fans . Illustrates control of topography by bedrock stucture and litl1ology.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Milici , R. c. , 1968, r� sozoic and cenozoic physiographic development of the lower Ternessee River: In terms of the dynamic equilibriuw concept: Journal of Geology, v. 76 , p. 472-479 . The Tennessee river is regarded as a trans-Appalachia� river that fonned on a coastal plain of Pennsylvanian sediments, probably early in the Mesozoic. The river may have had an initial consequent course close to its present course , and lat£ral migration southward off of the Nashville dome is postulated as the mechanism for entrapment of the river in Sequatchie Val ley.

Miller, A. M. , 1915, Wind gaps : Science, v. 42, p. 571-573. Suggests that , rather than indicating the former presence of a stream, the vast majority of wind gaps are simply cols in the top of the divide , notched by the retreat of the sources of two streams which have happe�ed to head opposite each other .

Miller, B. L. , 1939, Northampton unty, Co Pennsylvania: Geology and geography: Pennsylvania Geological Survey, 4th series, Bulletin, v. C48 , 496 p. Chapter on physiography, p. 115-158, contains most pertinent discussions . Includes physiography , erosion cycles, strea�, floods, drainage evolution, and wind gaps .

Miller, E. v. , 1985, Techniques for graphical and digital slope stability analysis developed for the Appalachian Valley and Ridge physiographj � province - case study : Giles County, VA [Abstract]: Geological Soc�ety of America Abstracts with Prog1ams, ·•• 17 , p. 125. The generated slope mapwith categories of les3 than 15, 15-35, and greater than 35 degrees was used as a base mapon which areas of colluvium and area� of dip slopes were delineated to produce a slope stability map with 10 categories.

Miller, E. v. , and Hubbard, D. A. , Jr., 1986 , Selected slope categories and karst features map of Giles C�1nty, Virginia [Map, scale 1:50,000]: Virginia Division Mineral Resources Publication, v. 70, 1 p. Hap shows slopes greater than 35 degrees, between 15 and 35 degrees, and less than 15 degrees. Also shown are sinkholes, areas of subsidence , and cave openings.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mi ller, J. A. , 1987 , What does it take to make a geomorphically effective flood? Some lessonE from the Nov�mber 1985 flood in West Virginia, in Kite, J. s. , ed ., Research on the late Cenozoic of the Potomac highlands : SE Friends of the Pleistocene , p. 3-30. "Effective" means that a flood causes lapid and substantial change of existing landforms that cannot be accomplished by events of lesser magnitude and which cannot be reversed by the steady operation of normal geologic processes over a period of at least several years. 'lbe unusual impact of the 1985 flood is probably due to structural control of valley physiography : ridge-fonming sandstone units effectively prevent any syst��tic increase in valley width as drainage area increases. Ps an indirect indicator of power, reaches of streams were classifit� into one of 4 classes based on the severity of erosion. The severity of ?rosion was found to be related to a "synthetic unit stream powet " parameter based on average values of channel slope , valley width, .!.."rl peak discharge in that reach. Observations suggest that where bedrn�� gorges and constrictions alternate with slightly wider valley reac�es exhibiting some alluvial bottomland, conditions are optimal for juxtaposition of a highly erosive flow with a valley that is vulner�ble to erosion. The worst erosion class was always associated with expanding flow.

Miller, R. A. , and Maher, s. w. , 1972, Geologic evaluation of sanitary landfill sites in Tennessee : Tennessee Division of Geology Envi ronmental Geology Se ries, v. 1, 38 p. Discusses weathering and soil characteristics of chief bedrock formations .

Mi ller, R. A. , Troxell, J., and Leopold , L. B. , 1971, HyCrology of two small basins in Pennsylvania bP.fNe urban!zation : U.S. Geological Survey Professional Paper, v. 701-A, p. A8-Al7. Discusses drainage area-discharge relationships, downstream hyd raulic geometry, suspended sediment dctta, and flood plains and terraces .

Miller, R. A. , and Wiethe , J o. , JQ75, Landslides in the Nashville, Tennessee area - winter, 1975: Tenne.� see Division of Geology Environmental Geology Series, v. 3, 15 p. Most slides were in colluvium, which author describes.

Miller, R. L. , 1938, Preglacial course of the Delaware ·River: Pennsylvania Academy of Sciences Pro , �edings , v. 12 , p. 107-113. Concludes that the regional structure and the behavior of modern streams in the upper Delaware Valley strongly support the contention of Campbell and Da scom that the Delaware River formerly flowed through Culve r Gap in Kittatinny Mountain.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Miller, R. L. , &1d Ful ler, J. 0. , 1954, Geology &ld oil resources of the Rose Hill district - the fenster area of the Cumberl&ld ove rthrust Block-Lee Countl' • Virginia: Virginia Geological Survey Bulletin, v. 71 , 383 p. In Physiography section on p. 192-215, discusses erosion levels, drainage pattern, drainage evolution, &ld Powell River (including cutoff meanders, cutoff tributaries, and terraces ), and subsurface drainage features .

Mi ller, V. C., 1953, A quantitative geomorphic study of drainage basin characteristics in the Clinch Mountain area, Virginia &ld Tennessee [Ph.D. thesis] : New York , Columbia University, 135 p. �u antitative study of stream length , basin area, drainage density, basin circularity, bifurcation ratio, valley-side slope , &ld hyposometric curves were made of 2 kinds of topography : 1) dip and antidip slopes of Clinch Mountain; 2) 3 maturely dissected areas of homogeneous topographic facies &1d dendritic drainage , one of which is underlain by Copper Creek dolomite, a second by s&ldstone &1d shale of the Athens Formation, &1d a third by the shaly Pennington formation.

Miller, v. c., 1971, Geomorphic map of southweste .n Indiana : Indiana State University Department of Geography &1d Geology , Professional Paper, v. 2, p. 12-13. The key to the present topography is the Pleistocene history. The numerous nearly-level areas interspersed among the dissected uplands are partially filled valleys of pre-Pleistocene streams, the reaction of well integrated drainage systems to ice invasion in some instances &1d to outwash incursion in cthe.-s.

Mi llette , J. F. G., &ld Higbee , H. w. , 1958, Periglacial loess, I. Morphological properties: Americ�! Journal of Science, v. 256 , p. 284-293. A study of loess in the Susquehanna River valley &ld in Quebec, canada .

Mills, H. H. , 1977, Slope deposits on the north side of Little Pinnacle Mountain, south carolina : S.C. State Development Board, Division of Geology, Geologic Notes, v. 21 , p. 150-163. Three separate slope deposits of different ages are recognized on the north side of Little Pinnacle Mountain, South Carolina, and can be differentiated on the basis of soil profile development &1d clast weathering.

Mills, H. H. , 1978, Hillslope evolution on the Pennington Formation, central Tennessee: An illustration of dynamic equilibrium: Tennessee Acade:ny of Science Journal, v. 53, p. 150-153. Along the Cumberl&ld escarpment, slopes on the Pennington forma tion are covered with a mantle of coarse s&ldstone debris derived from the cap rock above &1d have an ave rage inclinatioq of 21 degrees. Once the cap rock is removed, however, the texture of the debris mantle becomes finer and the slopes decline . A linear relation was found bPtween the steepest slope angle on a hill and the vertical dist&lce of the hill top below the base of its former cap rock .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mills, H. H. , 1981, Boulder deposits and the retreat of mountain slopes, or, "gully gravure" revisited: Journal of Geology, v. 89, p. 649-660. Observations on mountains composed chiefly of shale and capped with Tuscarora Sandstone suggest that slopes retreat by a process similar to but different from Bryan 's (1940 ) "gully gravure ." Boulders protect hollow floors from erosion, so that storm runoff incises gullies along the margins of the bouldery deposits . Episodically, however, a catastrophic storm wi th a recurrence intervals on the order of 1000 yr mobilizes the boulde ry debris and deposits it in h�llows . The armored floor thus shifts laterally. Subsequently, new gullies are incised adjacent to the old ones. The result is the lateral migration of one or both walls of the hollow.

Mills, H. H. , 1981 , Some observations on slope deposits in the vicinity of Granafather Mountain, North Carolina: Southeastern Geology, v. 22, p. 209- 222 . Examines topographic relations and relative-age cha racteristics of two ages of colluvium on and near Grandfather Mountain.

Mills, H. H. , 1982, Long-term episodic deposition on mountain foot slopes in the Blue Ridge province of North Carolina : Evidence from relative-age dating: Southeastern Geology, v. 23 , p. 123-128 . on the basis of weathering characteristics, soil-profile development, and topographic relationships , foot-slope deposits in the Dellwood, Grandfather Mountain, and Bakersville quadrangles of North Carolina were dividad into several age groups . Then , based upon the weathering criteria percent clay, Munse�� hue , and clast �athering measured in the B2 horizon at 135 sites, discriminant analyses were performed for each area. Plots of the scores on the resulting discriminant functions show discontinuitiPs between the youngest and next older age group in all three areas.

Mills, H. H. , 1982, Piedmont-cove deposits of the Dellwood quadrangle, Great Smoky Mountains , North Carolirz. , u.s.A. : Morphometry: zeitschrift fur Geomorphologie, v.26, p. 163-178. The morphometry of 34 fan-like deposits and their drainage basins in the Dellwood quadrangle of the eastern Great smoky Mountains was investigated. Fan variables measured included area, mean slope , upper-fan slope, length, width, and relief. Drainage-basin variables included area, mean slope, length , relief, and relative relief. Results were compared to those reported for arid-region alluvial fans and pediments .

Mills, H. H. , 1983, Clast-fabric strength in hillslope colluvium as a function of slope angle: Geografiska Annaler, v. 65A, p. 255-262. Clast orientation was measured in the upper 20 em of soil at 16 sites on forested hillslopes ranging from 9 to 42 degrees. Most sites displayed a significant fabric, with long axes parallel to slope and imbricated uphill . Fabric strength is greater on steeper slopes.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mi lls, H. H. , 1983, Pediment evolution at Roan Mountain, North Carolina , U.S.A. : Geografiska Annaler, v. 65A, p. 111-126 . Three ages of pediment-fan terraces were mapped, based on morphology and weathering characteristics. Results show that most terraces are unpai red and that the cross-fan sequencP. of terraces is either irregular or that younge r terraces tend to abut valley walls. The terr�ces dppear to be the result not of cyclic erosion and deposition produced by Quaternary climatic change , but of rc��rring stream capture and lateral erosion on the mountain piedmort. The regression equation of fan area on drainage-basin are� is similar to those reported for arid-region alluvial fans .

Mills, H. H. , 1984 , Effect of hillslope angle and substrate on tree tilt, and denudation of hillslopes by tree fall: Physical Geography, v. 5, p. 253- 261 . Measurement of tree tilt showed that trees on steep boulder streams are tj lted more than those on nose& or side slopes with similar �:ope &lgles, �� t this difference could result from a difference in tree types. On one very steep (39-degree ) slope, however, tilt of all types of trees is great, the ave��ge being 29 .1 degrees. In a second study, the volumes of all tree-fall pits within a 4-hectare area on a steep shale nose were measured , and an erosion rate of 13 mm/1 000 yr calculated .

Mills, H. H., 1985, Descriptions of backhoe trenches dug on New River terraces between Radford end Pearisburg, Virginia, 1981: u.s. Geological Survey Open-file Report, v. 85-474 , 67 p. Describes sediments , including �rticle size analyses , in trenches dug on terraces of New River ranging in elevation above modern river low-flow level from 5 m to 73 m. Photos are in color .

M1lls, H. H. , 1985, Description of stone-stripe excavation on Big Mountain, Giles County, Virginia: u.s. Geological Survey Open-file Report, v. 85-445, 11 p. Describes sediments and structures exposed by backhoe trench across the trend of a stone stripe located in a gap on Big Mountain, Vi rginia.

Mills, H. H., 1986, Downslope movement oi in situ clasts on foresLed hillslopes, Vi rginia: EarL� Surface Proces�es and Landforms , v. 11, p. 451-456 . Downslope movement of 109 clasts ranging in intermediate diameter from 30 to 870 mm �re monitored over a five-year period. radients ranged from 8 to 42 degrees. Regression on slope tangent, depth of clast base below ground surface , clast size, and clast sr�pe explained 70 percent of clast-movement variance .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mi lls, H. ri. , 1986, Piedmont-cove de Jellwood quadrangle, Great Smoky Mo;mtains , North Carolina , U.S.A dspech Jf sedimentology and weathering: Biuletyn Peryglacj�ln1 , v. 30, p. 91-109. A study of the textur� , �bble-roundness, clast-fabric, and sedimentary structures of f00t-slope deposits reveals little evidence of relict gelifluction . A discriminant analysis based on three weathering indices shows that younger deposits form a discrete group separated frore ol0er deposits by a hiatus in weathering intensity.

Mills, H. H. , 1986 , Possible differential �plift of New River terraces in southwestern Virginia: Neotectonic�, "'· 1, p. 75-86 . Frequency distributions of point �levations of alluvium-covered areas along the New River wre determined. 'lhe Radford North quadrangle shows a bimodal frequP.ncy ol�tribution, w� th alluvial deposits abundant at 0-12 m above modern river level (AMRL) and 30-49 m. 'lhe frequency distrlbution for �� e Pearisburg quadr�ngle is also bimodal, but the higher mode is centered at 67 � AMRL, 27 m above that of the Radford North quadrangle . One explanat'on is differential uplift of the Pearisbu rg area relative to tne Radfor� North area, which is consistent with probable movements .J faults associated with the Giles County seismic zone that separat�s the two arr"as.

Mills, H. H. , 1987 , va t:.ation in sedimentary properties of colluvium as a function of topographic setting , Valley and �idge province, Virginia : Zeitschrift fur Geomorphologie, v. 31, p. 277-292 . Mountain slopes in the study ar�a can be divided into 5 topo graphic settings that differ in sedimentary properties of colluvium: upslope noses, downslope noses, side slopes, moist, north-facing hollows, and other hollows . Colluvium on downslope noses appears to be oldest, that on upslope noses next oldest, and that ia hollows ar. :l on side slopes being youngest. Age differences may result from the manner in which hillslope topogtaphy evolves.

Mi UG, H. H. , Brakenridge , G. R., Jacobson, R. B. , Newell, w. L., Pavich , M. J., and Pomeroy, J. S., 1987, Chapter 2, Appalac�ian mountains r.ndplatea us, in Graf, w. L. , ed., Geomorphic systems of North America (GeolOtJical Society of America Centennial Special Volume ): Boulder, co, Geological Sc�iety of America , p. 5-50 . Contents include a brief outline of the history of geomorphology in the Appalachians, structural geomorphology in the valley and Ridge province , weathering ��d �rosion in the Piedmont cumpared to that on thE inner Coastal Plain, landslides in the Appalachian Plateau, debris avalanches and fan� in the Blue Ridge , stream morphology and chronolcgy in the Appalachians.

Mills, H. H. , and Delcourt, P. A. , 1989, Chapter 15, Appalachian Highlands and Interior L� P�ateaus, in Mo rrison, R. B. , ed ., 'lhe Geology of North J\me rica : v. K-2 , Quaternary nonglacial geology: Boulder, co, Geological �ociety of America. Summari?es research in or related to Quaternary geology in eact of �he unglaciated �lachian provinces, plus tl;e Interior Low Plateau .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mills , H. H. , Knox , L. w. , Bogle , F. R. , and Carter, K. B. , 1984 , Imminent cutoff of an ingrown steam meander �� d ongoing capture of a stream by its tributary at Window Cliffs, Putnam County, Tennessee : Tennessee Tech Journal , v. 19, p. 4-13. A razor-sharp 35-meter-high-divide at the neck of an ingrown meande r at Window Cliffs reprEsents the final stage in the abandonment of an incised meander. Seve ral hundred meters southwest of Window Cliffs, Cane Creek has migrated westward until it is separated from a tributary, Phelps Branch, by a narrow divide . At �� is point Phelps Branch is about 10 m lower than Cane Creek, and water is being diverted from the latter via a cave system.

Mills, H. H. , and Starnes, D. D. , 1983, Sinkhole morphometry in a fluviokarst region: eastern Highland Rim, Tennessee , U.S.A. : Zeitschrift fur Geomorphologie, v. 27, p. 39-54 . Multiple regressions of sinkhole variables agai nst 6 measures of drainage-basin size show that variables related to sinkhole horizontal si ze have relatively strong relationships to basin size (R-square values ranging from .474 to .621), whereas variables related to sinkhole depth or mean flank &lope have only weak relationships to basin size (R-square values :xnging from .104 to .206). The planimetric size of sinknoles having larger drainage basins apparently grows faster than that of sinkholes having smaller basins. The vertical size apparently is controlled by local bedrock conditions .

Mills, H. H. , Starnes, D. D. , and Burden, K. D. , 1982, Predicting sinkhole flooding in Cockeville: Tennessee Tech Journal , v. 17 , p. 1-19 . Sinkholes within the Cookeville ci ty limits were delineated on specially prepared 1:2400 topographic maps , and the characteristics of each recorded . Characteristics included morphometry of the sinkhole and its tributary basin, the tYFe of sinkhole, the hydrol0gic condi tion, the presence or absence of man-made structures, and whether or not there is evidence of ; loading. Th is infoPnation, together with preliminary estimates of ach sinkhole likely to be flooded by a 4-inch rainfall (assuming 100 percent runoff and impervious sinkhole floors), provides a basis for zoning areas likely to be subject to sinkhole flooding.

Mills, H. H. , and Wagner , J. R., 1985, Long-term change in regime of the New Rivet indicated by vertical variation in extent and weathering intensity of alluvium: Journal of Geology, v. 93, p. 131-142. A statistical analysis of New River te rrace elevations showed that alluvial deposits are more abundant at 0-12 m and 30-49 meters above modern river level (AMRL) , while the 12-30 m interval has relatively few deposits . Munsell cclor , particle-size distribution, and point counts of heavy and light minerals were made at 35 sites . These properties indicate a dramatic increase in weathering intensity between 20-30 m AMRL, corresponding to the break between lower and higher terraces .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Minard, J. P. , and Rhodehamel, E. c., 1969, Q'Jatern.- ry ge.:.logy of part of northern New Jersey and the Trenton arec , in Subitsky, S., ed ., Geology of selected areas in New Jersey and e�stern re•msylvania and guidebook of excursions : New Brunswick , Rutgers Unive rsity Pre�s, p. 279-313. Discusses Quaternary glacial deposits of the northern glaciated part of the state , and fluviatile and marine deposits of the ungla·i�ted southern part of the state .

Miotke , F. D., and Palmer, A. N. , 1972, Genetic relationship between caves and landforms in the Ma!Tiroth Cave National Park area: wurzberg, w. Germany , Bohler, 69 p. Cavern development in Mammoth Cave National Park has been controlled by the erosional and depositional history of the Ohio River drainage system during the late Te rtiary and Pleistocene . Major cave levels were formed where the entrenching Green River stood at base level for long periods, and therefore the largest cave passages correlate with terraces in the nearby river v�lley. Attempts to relate cave levels and sediments to each of the four classical glaciations.

Miotke , F. D. , and Papenberg, H., 1972, Ge0100rphology and hydrology of the Sinkhole Plain and Glasgow Upland , Central Kentucky Karst; preliminary report: Caves and Karst, v. 14, p. 25-32 . D1scusses first dye tracing of the Sinkhole Plain near Mammoth Cave National Park . Notes that the initial fluvial drainage pettern of the Sinkhole Plain still influences the subterranean drainage system. The Sinkhole Plain has a complex fluvial-karstic origin.

Miser, H. D., 1950, Manganese deposits of the southeastern United States, in Snyder, F. G. , ed ., Symposium on mineral resources of the southeastern United States, 1949, Proceedings : Knoxville, TN, U. of Tennessee Press, p. 152-169. On p. 158-160, discusses origin of manganese deposits, and relates origin to development of residuum and surficial deposits.

Mixon, R. B. , and Newell, w. L. , 1976, Prelim1nary investigation of faults and folds along the i�;er edge of the Coastal Plain in northeastern Vi rginia : U.S. Geological Survey Open-file Report, v. 76-330, 18 p. Detailed mapping has delineated northeast-trending flexures and faults which coj ncide with the segment of the Fall Line �ralleled by the Potomac River estuary. Deformation has produced a down-to-the-coast displacement of Coastal Plain strata and the underlying crystalline rocks. Although most of the displacement took place in the Cretaceous or early to middle Tertiary, displacements along these structures have appreciably affected the present distribution and thickness of Cc �al Plain units as well as the geomorphic history.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Mixon, R. B. , and Newell , w. L. , 1977, Stafford fault system - structures documenting Cretaceous and Tertiary deformation along the fall line in northeastern Virginia: Geology, v. 5, p. 437-440. Northwest-dipping , high-angle reverse faults have been mapped along the inner edge of the Coastal Plain. Although displacements are small (15 to 60 �) . the structures markedly affect the present distribution and thi ckness of Ccastal Plain sediments. The amount of displacement on the structures increases downward, indicating recurrent movement. The major deformation took place in the Cretaceous and the middle (?) Tertiary, but some latest Tertiary or Quaternary movement is possible.

Mixon, R. B. , and Newell, W. L. , 1978, The fault�d Coastal Plain margin at Fredericksburg, Virginia: Tenth annual Virginia field conference , Oct . 13- 14, 1978 : Reston, VA, u.s. Geological Survey, 50 p. Briefly describes stratigraphy of area, then provides sketches of several Cretaceous-cenozoic fault displacements exposed in the area.

Mixon, R. B., Powers, D. s. , and Daniels , D. L., 1984 , Buried Triassic basin edge and associated Cenozoic deformation, northern Virginia Coastal Plain [Abstract ): Geological Society of America Abstracts with Programs , v. 16, p. 180-181. The combination of a well defined Triassic basin edge in the subsurface and a thin Coastal Plain cover, including strata of Cretaceous and early and late 'fe rtiary ages, is a good framework for examing the nature and timing of Mesozoic and Cenozoic deformat;on in the inner Coastal Plain. Rock units directly overl::ring the buried early Mesozoic basin edge are folded into -, low-relief syncline-anticline pai r. Structural relief on lower Tertiary beds across the anticlinal structure ranges from 40 to 80 feet or more. Strata at least as young as middle Miocene have been folded to some degree.

Moneymaker, B. C., 1929, The caves of east Tennessee [M.S. thesis]: Knoxville, university of Tennessee, 63 p. Describes some well known caves.

Moneymaker, B. C., 1939, Erosional effects of the Webb Mo��tain (Tennessee ) cloudbur�t of August 5, 1938: Tennessee Academy of Sciences Journal , v. 14, p. 190-196 . Describes landslides , gully erosion, channel erosion, and channel deposition that resulted from a cloudburst of greater than 12 inches in 4 hours .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Moneymaker, B. C., 1941, S•hriver solution cavities in Tenn�ssee Valley: Journal of Geology, v. 49, p. 74-86 . Deep core borings and deep open-cut excavations in the Tennessee River reveal the presence of solution cavities 100 ft below the bottom of the Te.messee River. It is concluded that the solution of carbonate rocks within the zone of saturation is a normal geologic process .

Moneymaker, B. C., 1948, Some broad aspects of limestone solution in the Tennessee Valley: American Geophysical union Transactions , v. 29 , p. 93- 96. Deep borings made in the subsurface exploration of dam sites ar.d large open cuts made at dam construction projects reveal that solutional openings , some cavernous in dimensions , are present to depths of hundreds of feet below the present water table . In the development of such cavi ties , geologic structure is of greater importance than the chemical purity of the limestone . Notes that in the vicinity of Kentucky Dam, the extensively jointed Ft. Payne Formation is much more cavernous than the less jointed pu re limestone formations a few miles away .

Moneymaker, B. C., and Leonard, G. K., 1949, Geology and foundation treatment , Tennessee Valley Authority projects: Tennessee Valley AUthority Technical Report, v. 22, 548 p. Excellent descriptions of many dam sites, including sketches. Occasionally gives depths of alluvium and residuum, but not systematically. Appendix A (p. 511) discusses the Great Falls leakage problem, in which a reservoir leaked via solution channels through the ne<"lt of an incised meander in the Ft . Payne Formation.

Moneymaker, B. C., and Rhoades, R. , 1945, Deep solution channel in western Kentucky: Geological Society of America Bulletin, v. 56 , p. 39-44. Most solution occurred below the water table . Solution zones are of two kinds : 1) tabular bedding plane channels, and 2) enlargements of near-ver Lical joints. Excellent diagrams of these . Findings demonstrate that extreme solution may occur even in impure limestones unde r conditions of favorable structure, a continuous supply of moving water, and a long interval of time.

Monmonier, M. s. , 1967, Upland accordance in the ridge and valley section of Pennsylvania [M.S. thesis]: university Park, PA , Pennsylvania State university, 58 p. Low-order polynomial regression surfaces were calculated to measure topographic accordance and to determine regional trends. Two kinds of uplar.ds were sampled, the ridge tops and the local broad uplands . The percentage of the variation in elev, �on that a trend surface can explain is a measure of topographic accordance . Accordance of the local broad uplands is appreciably greater than that of the ridge tops, and is consistent with the concept of a high-level erosion surface . The trend maps indicate that the accordance is strongly assoc.1ated with present drainage , a result consistent with both peneplanation and no-peneplanation hypotheses.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Moore, D. w. , 1972, Geomorphology of the Deep River drainage basin and the carthage area, North Carolina [M.S. thesis]: Chapel Hill, NC, University of North Carolina , 83 p. Map and field observation indicate that the ancestral conse-

� . ·t Deep and Rocky Rivers wh ich flowed southeast on a low-relief Pi��'nt surface were captured by a lateral subsequent tributary of the ancestral Haw River. A calculated rate of denudation based on loads of several Piedmont streams, adjusted for effects of man on loads plus possible lowering of divides indicates that about 2-3 million years were requi red to erode the modern Deep River drainage basin from the older and higher erosion surface .

Moo re , D. w. , 1974, Denudation of the Deep River drainage basin and adj acent Fall zone , North Carolina [Abstract ]: Geological Society of America Abstracts with Programs, v. 6, p. 382 . See abstract of thesis (Moore, 1972) for content .

Moore , F. M. , and Myl roie, J. E., 1979, Influence of master stream incision on cave development , Trigg County , Kentucky, in Myl roie, J. E. , ed ., Western Kentucky Speleological Survey Annual Report: w� stern Kent . Speol . Surv., p. 47-68 . The incision of Sinking Fork into the plateau surface resulted in cave development through subsurface self-pi racy and subsurface capture of tributary streams . Diagrams sh�· history of cave development . Demonstrates that self-piracy by meander cutoff, or by larger-scale conduit formation, can in turn affect previously established tributary caves and meander-cutoff caves.

Moore , G. K. , 1973, Hydraulics of sheetlike solution �avities: Ground Water, v. 11, p. 4-11. The sheetlike solution cavities that supply water to most wells in central Tennessee are 100 to 2,500 ft wide and less than 0.2 inch high. Discusses mathematical techniques of estimating cavity dimensions from pumping tests.

Moore , H. L. , 1976, Drainage problems in carbonate terrane of east Tennessee , in Highway Geology Symposium, Orlando, Florida, May 19-21, 1976, Proceedings, p. 111-131 . Discusses piping failures in residuum over limestone and remedial actions . Three case histories in east Tennessee are discussed .

Moore , J. D. , 1972, Limestone hydrology and environmental geology, in Guidebook to Alabama Geology, Geological Society of America Southeastern Section, Guidebook 21-4 : Geological Society of America. Guidebook with examples of sinkholes and �inkhole subsidence .

Moravec, G. F. , 1974, Development of karren karst forms on the Newala Limestone in the Cahaba Valley, Alabama, in Rauch, H. w. , and We rner, E. , eds. , Fourth conference on karst geology and hyd rogeology , proceedings : p. 113- 121. Karren forms identified include rill karren, runnel karren, round karren, meander karren, cleft karren, solution basins, and scallops . TWo localities particularly favorable to formation are described.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Morisawa , M. , 1963, Distr�bution of stream-flow direction in drainage patterns : Journal of Geology, v. 71 , p. 528-529 . Actual distribut1on of stream direction of streams measured in sample basins of dendritic drainage pattern shows a close approximation to a tJ heoreti�al random distribution. Deviations from this ideal nistribution of stream-fluw direction occur in drainage systems where either a steeply sloping ground surface or rock schistosity is present .

Morisawa , M. E. , 1959, Relation of quantitative geomorphology to stream flow in representative watersheds of the Appalachian Plateau province (U.S. Office of Naval Research, Project NR 389-042, Columbia University Technical Report no . 20): New York, NY, Columbia University, 94 p. Objectives were 1) to deve�0p regression equations between peak flows and quantitative geomorphic factors, and 2) to place the regional description of the Appalachian Plateau on a quantitative basis. Results: A regression of peak intensity of runoff on basin area, rainfall intensity and frequency, and topography has a high correlation coefficient. Morphometry supports separation of the province into 3 divisions on the basis of stream lengths and drainage density. Basin geometry conforms to Horton's laws of drainage composition in ho rizontal , but not in vertical , properties.

Morisawa , M. E. , 1962, Quantitative geomorphology of some watersheds in the Appalachian Plateau: Geologica� Society of America Bulletin, v. 73, p. 1025-1046 . Geometry of 15 watersheds conforms to Horton's laws of drainage composition in horizontal but not in vertical properties. Geologic structure and varying lithologies interact to change vertical form elements and cause deviations from Horton's laws . Geometry provides quantitative and qualitative bases for grouping the regions studied into three distinct sections . A rr · -ession of peak intensity of runoff on basin area, rainfall intens��y and frequency, and topography has a high correlation coefficient.

Moss, J. H., 1976, Pe riglacial or:gin of extensive lobate colluvial deposits on the south flank of Blue Mountain near Shartlesville and Strausstown, Berks County, Pennsylvania: Pennsylvania Academy of Sciences Proceedings , v. 50, p. 42-44. TWo lobate sheets of scattered quartzitic cobbles and boulders extl·nd more than 2 miles across Martinsburg shale from cliffs of TUscarora quartzite. These deposits mantlt interfluves which grade upward into the nWbble-strewn slopes of Blue Mountain. The mountain slope is steplike , with risers becoming more sub:iued downslope . Blocks are most prominent on the outer edge of each tread. Evidence of at least two periods of block movement .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Moss, J. H. , and Kochel, R. C., 1978, unexpected geomorphic effects of the Hurricane Agnes stonn and flood , Conestoga drainage basin, southeastern Pennsylvania: Journal of Geology, v. 86, p. 1-11. Authors addressed two questions : 1) why was massive flooding caused by such a relatively small total ra' :all, and 2) why did thi s catastrophic event cause only minor geomorphic changes? Note that the effect of the flood, having a several hundred year recurrence interval, was to trans�rt large quantities of fine sediment out of the basin but not to alter significantly the shape of channels or contours of floodplains .

Mundorff, M. J. , 1950, Flood-plain deposits of North Carolina Piedmont and mountain streams as a possible source of ground-water supply: North Carolina Department of Conservation and Development, Division of Mineral Resources Bulletin, v. 59, 20 p. Provides logs of 21 test holes drilled into flood plains in the �tudy area. Has map showing major flood-plain deposits for all of "'o rth carolina.

Myl roie, J. , and Dyas, M. , 1985, We stern Kentucky region, in Doughe rty, P. H. , ed ., caves and karst in Kentucky: Ken . Geol . surv. Sp. Pub. 12, Ser . XI : Lexington, KY, Kentucky C� ological Survey, p. 119-145. Describes .aajor cave systems in western Kentucky.

Neal , w. P. , 1967, The southern Piedmont upland of the southeastern United States: A geomorphic system in a steady state of dynamic equilibrium [l1.A. thesis]: Athens , University of Georgia, 81 p. Discusses geomorphic processes in the Piedmont , equilibrium changes, and evidence for the Piedmont being in a state of dynamic equilibrium. Best part is map showing variation of regolith thickness in Whiteall watershed, Georgia , determined from 50 bore holes.

Nea ry, D. G. , and SWi ft, L. w. , 1984, Rainfall thresholds for triggering a debris avalanching event in the southern Appalachians [Abstract]: Geological Society of America Abstracts with Programs , v. 16 , p. 609 . Discusses rainfall totals and intensities from 15 gauges of a stonn that set off debris avalanches in Pisgah National Forest.

Neary, D. G. , and SWi ft, L. W. , Jr. 1987, Rainfall thre3holds for triggering a debris avalanching event in the southern Appalachian Mountains , in Costa , J. E. , and Wieczorek , G. F. , eds., Debris flows/avalanches: Process, recognition, ant mitigation : Geological Society of America Reviews in Engineerinr. Gee��' v. 7: Boulder, 00, Geological Society of America, p. 81-92. Analyzed charactP.ristics of Novembe r, 1977, stonn that set off debris avalanches in North carolina Blue Ridge . The re was high antecedent rainfall , then relatively continuous and even (20-50 lllll(day) for 3 days . '!his was capped by intense convective downpours that produced avalanches. Many gauges exceeded 75 mm/hr, indicating return intervals of 50-200+ yr . Stream flows had return periods ranging from 20 to 100+ years. Volume of material averaged 2,500 cubic meters per avalanche .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Nelson, B. w. , 1965, Erosional equilibrium in the Piedmont Plateau [Abstract ]: Geological Society of America Special Paper , v. 87 , p. 116-117 . Notes that the slope of the Piedmont upland is adjusted everywhere to the erosional equilibrium that presently exists in the smallest tributary basins rather than to the slope of an olde r rejuvenated peneplain.

Newell, W. L. , 1970, Facto1s influencing the grain of the topography along the ;o7illoughby Arch in northeastern ve rmont: Geografiska Annaler, v. 52A, p. 103-112 . !;ays t!1e eftect of glaciation on the topography has been minor . The topography was adjusted to the orientation of bedrock fractures before the Pleistocene , probably as a result of chemical erosion. Compared equal-area plots of maximum slope linears and similar plots for joint systems .

Newell, w. L., 1977, Surficial geologic maps of the Beattyville, Campton , and Hazard North quadrangles, Kentucky River Area Development District, Eastern Kentucky [Map] : U.S. Geological Survey Miscellaneous Field Studies Map, v. MF-843, 2 p. Mapunits include residuum (greater and less than 5 {t ), colluvium (thin [less than 5 ft] and discontinuous , thin and continuous , and thick [greater than 5 ft] ), alluvium (modern channel and flood-plain alluvium, low-level terrace alluvium, and high-level terrace and abandoned terrace remnants ). Scale is 1:24 ,000.

Newell, w. L. , 1978, understanding natural systems : A perspective for land-use planning in Appalachian Kentucky: u.s. Geological Survey Bulletin, v. 1438, so p. Explains bedrock control of geomorphic processes, distribution and significance of surficial deposits, and hydrologic characteristics of the terrain. Geomorphic processes and the landscape may be evaluated in terms of low to high risk potential , thereby indicating both opportunities and limitations for land use . Contains several nice landscape sketches.

Newell, W. L. , 1973, Upper Te rtiary :md Quaternary stratigraphy in the Frede ricksburq. area, in Mixon , R. B. , and Newell, w. L., eds., The faulted Coastal Plain margin at Fr�ericksburg, Virginia (Tenth Annual Vi rginia Geology Field Conference ), p. 44-47. Briefly C:escribes J.ate Te rtiary and Quaternary stratigraphy, including the ··u�land 9ravel" and the Rappahannock River terrace deposits, and their �cobable structural control .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Newell , w. L. , Pavich, M. J., Prowell, D. C., and Markewi ch, H. W. , 1980, Surficial deposits , weathering processes, and evolu�ion of an inner Coastal Plain landscape , Augusta, Georgia, in Frey, R. W. , ed ., Excursions in sout��astern geology, Geological society of America 1980 Annual Meeting, A-:.lanta , Georgia: �'alls Church, VA, American Geological Institute, p. 527- 544. Inner Coastal Plain landscape has been evolVlng since the middle to late Tertiary. Multiple weathering horizons are interpose1 between sequential deposits. Because of differences in permeability and erodibility, surficial deposits on the Coastal Plain have much longer residence times than those on the Piedmont . At the Fall Line , the Piedmont surface is lower than that of the adjacent Coastal Plain.

Newell , W. L., Prowell, D. C. , and Mixon, R. B., 1976 , Detailed investigations of a Coastal Plain-Piedmont fault contact in northeastern Vi rginia: u.s. Geological Survey Open-Fil? Report, v. 76-329, 14 p. A trench exposed a high-angle reverse fault juxtaposing Paleozoic Quantico Slate and Cretaceous Potomac Group rocks. Cross-cutting relations and stratigraphic details indicate that the subsidiary faults in the Cretaceous rocks document a history of episodic deformation, in part active du ring accumulation of the Coastal Plain strata .

Newell , W. L. , and Rice, D. D. , 1978, Structural control of the CUmberland River and its anceatral channels at Flat Lick, Kentucky : Journal of Research of the u.s. Geological Survey, v. 6, p. 359-367 . Distribution of alluvium as high as 76 m defines t� ancestral channels of the CUmberland River. The oldest channel is on the north flank of the Flat Lick anticline , the second oldest is superimposed on the crest, and the modern channel is entrenched in the south-dipping limb of the fold . This sequential pattern can be explained in terms of structural and lithologic constraints upon fluvial processes wi�hout recourse to contemporaneous tectonism.

Newman , w. s., Cinquemani , L. J., Pardi, R. R. , and Marcus, L. F. , 1980, Holocene delevelling of the United States' east coast, in Morner, N. A. , ed., Earth rheology, isostasy, and eustasy, proceedings of a symposium, Stockholm, 1977: New York, NY, Wiley, p. 449-463. Repeated levelling surveys, tidal gauge analyses, and sea-level data indicate that the east coast of the u.s. has suffered a complex deformational pattern during Holocene time. Deformational factors probably include glacio-isostasy, hydro-isostasy, peripheral bulge movements , geosynclinal subsidence , and sediment loading.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Newton, J. G. , 1976, Early detection and correction of sinkhole problems in Alabama, with a preliminary evaluation of remote sensing appl ications : Alabama Highway Depart�nt Research Report, v. HPR-76 , 83 p. Induced sinkholr:s result from a decline in the water table due to ground-wate-r withdrawals and from construction. An estimated 4, 000 sinkholes and related features have formed in Alabama since 1900. Almost all induced sinkholes C>Ccur where cavities develop in residual or other unconsolidated deposits overlying openi ngs in carbonate rocks . Low-level photography is useful in detecting incipient sinkholes .

Newton, J. G. , 1981 , Induced sinkholes : An engineering problem: Journal of the Irrigation and Drainage Division, Proceedings of the American Society of Civil Engineers, v. 107, p. 175-185. A brief summary of previous publications. Some features that indicate the development of induced sinkholes: circular and linear cracks or fractures, appearance of depressions, slumping or sagging of structures, small conical holes that appear in the ground in a relatively short period of time , and 14 others .

Newton , J. G. , 1984 , Sinkholes resulting from ground-water withdrawals in carbonate terranes : An ove rview , in Holzer, T. L., ed ., Reviews in Engineering Geology: Boulder, co, Geological Society of America, p. 195- 202. Suggests that identifying the terrane in which sinkhole activity most c0111110nly occurs and limiting large withdrawals of water from it will eliminate or minimize the problem. The terrain, youthful in nature , exhibits little karstification, is usually a lowland area, has a wa ter table above or near the top of bedrock , and contains perennial or near-perennial streams .

Newton , J. G. , Copeland, c. w. , and Scarbrough , w. L., 1973, Sinkhole problem along proposed route of Interstate Highway 459 near Greenwood, Alabama : Alabama Geological Survey Circular, v. 83, 63 p. More than 150 sinkholes, depressions, and related features have formed in or near the right-of-way. Development of sinkholes is restricted to an area underlain by the TUscumbia Limestone , lowermost beds of the overlying Floyd Shale, and in the immediate vicinity of faults.

Newton, J. G. , and Hyde, L. w. , 1971, Sinkhole problems in and near Roberts Industrial Subdivision, Birmingham, Alabama : A reconnaissance : Geological Survey of Alabama Circular, v. 68, 42 p. More than 200 collapses and areas of subsidence fomed in an area less than half a square mile during 1963-197C . A major lowering of the water table, as much as 140 ft, is responsible. The formation of sinkholes results from the collapse of cavities in residual clay that have been created by spalling or the downward migration of clay through openings in underlying carbonate rocks.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Nixon, R. A. , 1979, Weathering of the �anola Granite to gibbsite in an acidic environment - a model for bauxit� genesis [Abstract ): Geological Society of America Abstracts with rrograms, v. 11, p. 207. Relal i.onships suggest that more than a warm, humid climate is nece5sary tor bauxite genesis. An accumulation of organic matter is required, as well as permeable sediments .

Nixon, R. A. , 1980, Rates of chemical weathering of granite in an acidic envi ronment, P��ola Mountain, Georgia [Abstract ): Geological Society of America Abstrac�s with Programs , v. 12, p. 203. carbon-14 dates obtained from the soil were 4,995 yr BP at 1 ft below the &.lrface and 7,745 yr BP at 4 ft. Data imply that chemical weathering in the Georgia Piedmont takes from 10,000 to 100,000 yr to kaolinize a granite .

Nixon, R. A. , III, 1981, Rates and mechanisms cf chemical weathering in an organic environment at Panola Mountain, Georgia [Ph.D. thesis): Atlanta , �. Emory University, 182 p. Studied weathering in soil profile in colluvium mixed with organic .atter. From results, inferred the stability of granite in the Georgia Piedmont and the manner in which granitic landforms develop.

Nizinski, H. , 1969, Slope characteristics in Washington County, Pennsylvania, relative to local base level and exposure direction [M.A. thesis): Pittsburg, PA, University of Pittsburg, 70 p. We ak correlations exist between the ove rall slope angle and both exposure direction and local base level. Similar weak correlations exist between slope length a.nd local base level . Types of slope profiles also show only weak associations with these factors.

Nolting, J. P. , Jr., 1931, Drainage changes in the headwater region of DecY�rs Creek : west Virginia Academy of Scienc�s Proceedings , v. 5, p. 149-152 . Suggests that Deckers Creek is a relatively young stream which owes its present size and importance to the fact that it robbed ·�e Tygart River of part of the latter'�; headwaters. Piracy indicateri by its peculiar gradient , its br�b&J tribut�ries, the widened

valley, and the presence of alluvi•:..rn between it and Stony Run .

Nutter, L. J., 1969, Ground-water occurrence in the Maryland Pied:.ll·;nt: M." tyland Geological Survey Report of rr.·. estigations, v. 10, 56 p. Much of the ground wat,�r is stored in the saprolite, whicr ha s an average thickness of 45 rt . Many wells yield water occurring ;n joints, fractures , and other crevices in the rocks ; the occurrenr� and distribution of these features are difficult to predict, but the drainage pattern and surface topography of the Piedmont reflects the existence of major joint systems in the rocks.

Nuttar , L. J., 1974, Hydrogeology of Antietum Creek basin: Journal of Research of the u.s. Geological Survey, v. 2, p. 249-252 . Ground-water discharge of the basin is about 85 percent of total discharge, vs . 70 percent in two non-carbonate basins. Large quantities of ground wa�er are stored in a thick residual mantle. The major orientations of straight stream reaches along Antietam �reek and the strikes of major joint sets are nearly coincident .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 O'Leary, D. w. , 1972 , The form, structure, and avolution of the Allegheny Front in Centre County , Pennsylvania [Ph.D. thesis]: Un ive rsity Park , Pennsylvania Stat� University, 164 p. Di vided east side of Allegheny Plateau into 3 parts: Plateau , foothills, and forehills. A complex relationsh\p exists between joints and lineaments below the front, whereas simple joint control relates the two on the Plateau . Dissection of the front takes place by 1) headward eros; on of transverse streams into the front ; 2) pi racy of lateral Plate�u �treams by these transverse foothills streams; 3) acceleration of downcutting by pi rated lateral streams resulting in separat�on of parallel Plateau slices; 4) dissection of Plateau slices b� increased headward cutting of consequent transverse tributaries. Notes that colluvial banks, talus piles, and boulder trains represent static disequilibrium.

Oberlander, T. M. , 1985, Origin of drainage transverse to stucture in orogers, in Morisawa , M. , and Hack , J. T. , eds., Tectonic geomorphology: Boston, Allen & Unwin, p. 155-182. Di scusses origin of transverse drainage in the zagros , and briefly applies these observations to the problem of Appalachian drainge evolution. The principle to be de rived is the importance , after the initial stage of uplift and �rosion , of past outcrop patterns in controlling stream f��;qation. The present geological pattern is relevant only insofar as i� suggests prior patterns that could influence drainge evolution.

Obermeir, s. F. , and Langer, w. H. , 1986 , Relationships between geology and engineering characteristics of soils and weathered rocks of Fairfax County and vicinity, Virginia: u.s. Geological Survey Professional Paper, v. 13t �, 30 p. Consistently found a correlation between parent materials and engineering behavior. Discusses parent materials, soil structure, weatherir.g profile, engineering soil classification, surface and internal drainage characteristics, suitability as compacted material, excavation properties, susceptibilty to erosion, shear �trength and compressibility, allowable bearing pressure, slope stability, and road-performance characteristics.

Ogden, A. E. , 1974 , The relationship of cave passages to lineaments and stratigraphic ftrike in central Monroe County, We st Virginia, in Rauch, H. w. , and Werner, E., eds. , Conference on karst geology and hydrology, proceedings : Morgantown, WV, West Virginia Geol . & Econ . Surv. , p. 29-32 . Orientation rosette diagrams were prepared for both lineaments ar� for straight cave segments. The most common cave-�ssage otientation is parallel to the stratigraphic strike, although the lir,r.ament and cave-segment orientation distributions differ siqnificantly.

Ogd��. A. E. , 1982, Karst denudation rates for selected spring basins in Wf �st ''; rginia: �S Bulletin, v. 44, p. 6-10. Denudation rates for the springs were as follows: Dickson Spring, 22 .6; walters Spring, 22.3, and Cold Spring, 19.0 mmv1 000 yr . Based on sampling for a period of one year .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ogden, A. E. , and Ri' 1. w. , 1977, The effects of hyd rogeologic setting on the sto� res c of karst springs in Monroe Cc:�mty, We st Vi rg�nia, U.S. A. , in Tolson S., and Doyle , F. L. , eds . , International Association of Hydrogeologif 1emoi r 12 (Karst hyd rogeology] : Hunt:.wil'.e, AL, univ. Alabama at Hunt�ville, �· 363-376. Three "conduit" springs were mnitored in Octc�r, 1974, for discharge and water quality during the first major storm to follow a long dry period of base flow conditions . In general , the larger sp•:ing basins had higher peak discharges but lower ratios of peak '.:rJ base discharge . The ratio of maximum to minimum hardness was also lower for the larger spring basin areas; this shows that smaller basins exhibit flashier spring responses to storm events .

Ogden, A. E. , and Reger, J. P., 1977 , Morphometric analysis of dolines for predicting ground subsidence , Monroe County, We st Virginia, in Dilamarter, D. , and Csillany, S., eds., International Symposium on Hydrologic Problems in �arst Regions, Bowling Green, KY, 1976, Proceedings : Bowling Green, KY, t�e�t. Kentucky university Press, p. 130-139. Different formations within the Greenbrier limestone possess relatively distinctive doline distributions. The percentage of limestone area in dol inee and the doline density (number of dolines per square mile of limestoce ) arc useful indicators of areas of

potential subsjdence and .· furthe[II'Ore , coincide with total cave footage . A ground subsid�nce susceptibility map that combines areas of optimum hillslope steepness and percent area in dolines was prepared.

ulmstecl , F. H. , dnd Hely, A. G., 1962, Relation between ground water and surface water in Brand{Wine Creek basin, Pennsylvania: u.s. Geological survey Pr ofessional Paper, v. 417-A, 21 p. The seeming inconsistency between the cmall tomoderate ground-water yield to wells and the high yield to streams is explained in terms of the deep permeable soils, the relatively high gravity yield of the zone of wa ter-table fluctuation, the steep water-table gradients toward the streams, the relatively low transmissibility of the rocks, and the rapid decrease in gravity yield below the lower limit of water-·table fluctuation.

Olson, C. G. , and Hupp, c. R. , 1986, Coinc:idence and snatial variability of geol�·, soils, and vegetation, Mill Run watershed, Vi rginia: Earth SUrface Processes and Landf�rms, v. 11, p. 619-629 . Examination of the bedrock ge>:�logy, geOII'Orphology soils, and vegetation shows distinct distributional correspondenc es . On convex colluvial slopes, mixed har�xx3 forests are mJst common. In concave coves and deep gorges, mix� hardwoods ar� replaced by conifers. In thin colluvium, in poorly developed soils, and on block(ields, chestnut oak is sin�;larly prevalent. Conifers dominate shaley bedrock areas. Soils and surficial sediments have a major effect on near-surface hydrology. Vegetation is strongly dependent on water availability and thus reflects the distribution of subsurface barriers and sediment-soil facies change . "Soil welding" concept discussed.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Olson , c. G. , Ruhe , R. V. , and Maus::.:'\ch, M. J. , 1981, The terra rossa limestone contact phenomenon in kar(;t, SC'tthern Indiana : Soil Science Society of �rica Journal , v. 44, p. 1075-1079. Attacks the idea that terra rossa is a residu�l product from solution of limestone . First, the sharp. abrupt contact between the terra rossa (t.r.) and the limestone argues against this. In addition, the insoluble residue in the limestone is insufficient to account for the thickness of the t. r. Chemis�.:-y and clay minerals differ greatly in the t.r. and the rock . Suggests t.r. is mainly debris derived from erosion of higher lying clastic sedimentary rocks that has been transported and deposited on pediments cut into lO't.er lying limestone . This sediment subsequently weathers to terra rossa.

Oriel, S. S., 1950, �ology and mineral resourcef of the Hot Springs window, Madison County, Norl:h Carolina: North Carolin< Divislon of Mineral Resources Bulletin, v. 60, 70 p. Page 5 has a good discussion of the manner in which topography is conuolled by the geology in the study area.

Osterkamp, W. R. , and Costa, J. E., 1986, Denudation in selec::ed debds-flow basins, in Proceedingn of the Fourth Federal In�er�gency Sedimentation Conference , March 24-27 , 1986 , Las Vegas, Nevada : Interagency Advi. sory Commdttee on Water Data, p. 4-91 to 4-99. Denudation rates resulting fromdebr is flows in the Blu� Ridge Mountains in Nelson County, Vi�ginia (among other places) , were determined by measuring volumes and ages of deposits. 'lWo rates from Davis Creek tributary, Vi rginia, were 38 and 24 mmv1000 y� , much lower than sites in t�e western U.S. owing to the infrequency of debris flows . Authors note that if t�e debris is stored on lower slopes without entering the stream system, short-term sampling for sediment yield at streamflow gauges fails to rP.flect erosion in higher parts of the basin, and sediment-deliver.' ratios may approach zero.

Osterkamp, W. R., and Hupp, C. R. , 1984 , Geomorphic and vegetative characteristics alon·j three northern Virginia streams: Geological Society of America Bulletin, v. 95, p. 1093-1101. Prevalent alluvial surfaces identified were the depositional bar. the active-channel shelf, the flood plain, and terraces. Stages corresponding to active-channel-shelf levels were equivalent to flow durations of 5 to 13%. Stages corresponding to flood-plain levels were equivalent to discharges with 1.4 to 2.0-yr recurrence intervals. Each surface supports characteristic ·;pecies. Plant distributions appear to be largely controlled by t1ow frequency and intensity, so that plants may help to identify geomorphic levels and potential for fl� damage .

Otton, E. G. , Cleaves, E. T. , Crowley, w. P. , Kuff, K. I:{. , and Reinhat·dt , J., 1975, Cockeysville

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 OUterbridge , w. F., 1987, The Logan Plateau, a young phys iographic region in West Virginia, Kentucky, Vi rginia , and Tennessee : U.S. Geological Survey Bulletin, v. 1620, 19 p. The Logan Plateau is developed on the Breathitt and Kanawha Formations of Kentucky and West Virginia, parts of the New River and Pocahontas Formations of we st Virginia, and their stratigraphic equivalents in Virginia and Tennessee . Weathering averages 56 rn in depth on hilltops , but is shallow along vall�y sides . Based on stream loads , a reasonable figur� for the erosion rate of the subgraywacke sandstone, siltstone , shale , and coal areas is 100 rn;m.y. Orthoquartzite surrounding the Logan Plateau is eroding at a rate of 10 m;m.y. A contour map of hi�hest elevations indicates a probable former erosion surface whose age is about 1.5 rn.y. , based on the above erosion rates . Major streams were strongly affected by the establishment and history of the Ohio River. The Big Sandy River and the South Fork of the Kentucky River, in part' -ular , have been increasing their drainage areas by headward exte •..;ion and by stream piracy.

Outerbridge , w. F. , 1987 , Relation between landslides and bedrock in the central Appalachian Plateaus [Extended abstract ]: u.s. Geological Survey Circular, v. 1008 , p. 36-37 . Uses Jenkins 1 x 2 degree sheet as illustration. Table 14.1 lists rock types, in order of increas;ng tendency to fail, and their typical styles of failure , based on observations in eastern Kentucky. Excepting rock falls, rock topples, and block glides , there is very little bedrock involvement in landslides in the Appalachian Plateau. Landslides are confined to colluvium and to the very thin weathered zone above bedrock . The weathering characteristics of the unde rlying rock determine the characteristics and composition of the soil that forms . It is these characteristics that determine the type of land£lide.

Overstree� , E. F. , 1964, Geology of the Southeastern bauxite deposits: U.S. Geologic-'ll Survey Bulletin, v. 1199-A, p. Al-A19. In v:�lley and Ridge , formed on a Paleocene and Eocene land surface , represented by the Ha rrisburg or Valley Floor peneplain. Clay probably accumulated in shallow sinkholes and later weathered to bauxite . Preservation is due mainly to redeposition of bauxite and kaolin below the surface by collapse of underlying caverns in limestone soon after its deposition. Present distribution of deposits is restricted to fortuitous locations near divides or on remnants of terraces .

0\•e rstreet, w. C. , White, A. M. , Whitlow, J. w. , Theobald, P. K., Jr ., Caldwell , D. w. , and Cuppels, N. P., 1968, Fluvial monazite deposits in the southeastern United States: u.s. Geological Survey Professional Paper, v. 568 , 85 p. Excellent discussion of surficial deposits on p. 28-47. Discussion of colluvium is particularly good . Cross section� and logs of drill holes.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Owens , J. P. , 1970, Post-Triassic movements in the central �rd southern Appalachians as recorded by sediments of the Atlantic Coastal Plain, in Fisher, G. w. , and others, eds. , Studies of Appalachian geology: New York , Wiley, p. 417-427 . Prograding of clastic wedges into the depositional basin reflects structural activity in the sourceland. Recycling of material from the older Coastc.l Plain format!ons is minor. The movements of the carbonate-clastic boundary in the northern and southern Coastal Plain through time is shown in Fig. 7. The carbonate facies is much morg widespread in the southern Atlantic Coastal Plaln than in the northern, suggesting less uplift in the southern than in the central Appalachians during the formation of this sedimentary prism. Diastrophic movements in the central .� lachians were greater than in the southern, and appear to have been more irregular.

Palmer, A. N. , 1974, Geologic influence upon cave-passage orientati in

Ludington Cave , Greenbrier County, West Vi rgi.-;ia, in Rauch, H. V'i., and We rner, E. , eds., Fourth conference on karst geology and hydrology, proceedings : Mo rgantown, WV, West Virginia Geol . & Econ. Surv. , p. 33-40. Trunk passages �lon9 the Hillsdale-Maccrady co�tact are much more concordant with the structure than are the tributary passages. Most passages above the ccntact descend steeply across the structure. With only one major exception, ground-water flow has been strongly vac�se in tendency, descending along the sttepest availiable path under the influence of stratigraphic and structural c nditions .

Palmer, A. N. , 1975, The or:gin of maze caves: NSS Bulletin, v. 37, p. 57- 76 . Two common settings unde r which most maze development occurs: 1) where soluble rock receives diffuse groundwater recharge from the ove rlying surface or from and adjacent formation; 2) where g.w. in a cavernous region undergoes great variations in discharge and in hydraulic head, owing to flocdwater recharge . Case 1 generally occurs in karst aquifers capped by permeable but insoluble rock, or in isolated hills of soluble rock . In case 2, ponding occurs behind constrictions cru ring peak flow in active stream passages, resulting in the rapid development of blind fissures and diversion mazes .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pal�r, A. N. , 1977, Influences of geologic structure on ground-water flow and cave deve lopmer.t in Mammoth Cave National Park , in Tolson, J. s. , and Doyle , F. L. , eds., International Association of Hyd rogeologists Memoi r 12 [Karst hydrology ): Huntsville , AL, univ. Alabama at Huntsville, p. 405- 414 . Stratal dips and passage gradients are generally less than half a degree. Ground-water flow is highly concordant wilh the bedding of the limestone , and varidtions in �ave-passage gradients are achieved by a va riety of attitudes with respect to local dip di rections and by differences in dip magnitude . The varied lithology of the limestones and the prominence of their bedding-plane partings have caused much perching of ground water. The sinuous patterns of cave passages, particularly in the vadose zone , iF influenced primarily by irregularities in Jocal beddi�g structure. Fonner water tables and base levels are jiscernable as points where cave passages are reduced in gradient and lose their down-dip orientation. The underground flow systems have evolved from a few major drainage lines fed by sinking streams to a large m.unber of flow paths connected in branchwork patterns and fed by point sources of recharge such as sinkholes .

Palmer, A. N., 1981, A geological guide to Mammoth Cave National Park : Teaneck , NJ , Zephyrus Press, 196 p. Chapters 10 (How Mammoth Cave was formed ) and 12 (Evolution of the Flint Marnmcth CavP System) are most pertinent. Chapter 14 (A geological gu1Je �o tr3ils in Mammoth Cave ) is also useful . Good diagrams.

Palmer, A. N., 1984, Geomorphir interpretation of karst features, in LaF��ur , R. G. , ed ., Groundwater as a geomorphic agent: Boston, Allen & Unwin, p. 173- 209. Includes Appalachians, among other locations . Main section is "Recognition of the genetic environment of karst features." Field examples include "Histcry of changes in erosional base level : Mammoth Cave , Kentucky," and "Evolution of karst drainage and topography in a limestone plateau: Blue Spring Cave , Indiana ."

Palmer, A. N. , 1985, The Mammoth Cave reg1on and Pennyroyal Plateau, in Dougherty, P. H. , ed., caves and karst of Kentucky: Ken. Geol . Surv . Sp. Pub . 12, Ser. XI : Lexington, KY, Kentucky Geological Survey, p. 97-118. Discusses geological setting, relationship of karst and caves to the geological setting, hydrologic controls of =ave patterns, and relationship of karst to the local geomorphic history.

Palmer, A. N. , Palmer, M. V. , and White, w. B. , 1981, A guide to the historic section of Mammoth cave [Monograph ], in Beck , B. F. , ed ., Eighth International Congress of Speleology: Huntsville , AL, NSS , 59 p. Engl ish section is on p. 1-29. Table 1 shows minerals found in caves of the central Kentucky karst . Fig. 14 shows relation of zones of mineralization to position of passage with respect to caprock .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Palmer, A. N. , Powell, R. L. , and Moore , M. c. , 1973, The karst areas of Indiana , in NSS 1973 Convention Guidebook: Huntsville, AL, NSS , p. 3-10. Discusses physiography and development, stratigraphy and lithology of the karst-bearing units. Fig. 2 shows physiographic provinces of southern Indiana , Fig. 3 is sketch of idealized karst topography in the Mitchell Plain and Crawford Upland .

Pal mer, M. v. , 1976, The Mitchell Plain of southern Indiana : NSS Bu lletin, v. 38 , p. 74-79 . A topographic study . The Mitchell Plain is composed of 3 landform types and has been modified by at least 3 base-leveled surfaces which cut across the different landform types . Landform types are 1) areas of sinkhole plain, 2) areas of unconsolidated surficial cover, ar.� JJ areas of dissected upland . The base-level-controlled �urfaces include : 1) the uppe r Mitchell Plain surface , 2) the lower Mitchell Plain surface , and 3) the Blue River Strath. Fig. 3 is a landform map of southern Indiana . Fig. 4 provides cross sections .

Palmer, M. V. , and Palmer, A. N. , 1975, Landform develoJ;��ent in the Mitchell Plain of southern Ind1ana : Origin of a partially karsted plain: Zeitschrift fur Ge��rphology, v. 19, p. l-39 . Paper by M. V. Pc.lmer ( 1976 ) provides a sur.mary version of this paper . Of interest are distributions of 3 landform types as function of altituc1.e , distance u{>-dip from zero structural contour on the Salem Li�Qtone , and from major entrenched rivers. Also, distributions of altitude and depths of sinkholes in va rious locations. Al so, variation in sinkhole density within the stratigraphic section . Figure 13 shows relationship of altitudes and depths of sinkholes to horizontal dh.tance from the main stream passages of unde rlying caves. Fig. 15 shJNS relationship of sinkhole density to horizontal distance from cave passages .

Parizek, E. J., and Woodruff, J. F. , 1956, Apparent absence of soil creep in the east Georgia Piedmont : Geological Society of America Bulletion, v. 67, p. 1111-1115. Numerous vertical cuts show little suggestion of disturbance of veins and other near-verticQl linear features . Suggest stone lines are not formed in this manner, as suggested by Eargle (1940).

Parizek , E. J., and Woodruff, J. F. , 1957, Description and origin of stone laye rs in soils of the southeastern F�ates : Journal of Geology, v. 65, p. 24-34. Authors conclude that stone lines (which they name carpedoliths ) are former surface aggrega�ions �overed by sheet wash and colluvial deposits. Suggests a climatic change from one favorable to erosior. to one conducive to depositio� Because of the widespread extent cf stone lines, a high percentage of Piedmont soils appears to be colluvial raL,er than residual .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Parizek, E. J., and Woodruff, J. F. , 1957, Mass wasting and the deformation of trees: American Journal of Science, v. 255, p. 63-70. Notes that continuously slow-creeping soil and concomi tant tree growth should hypothetically develop trunks with a long sweeping curve from ground to terminal bud rather than the elbow-tx� curve and ve rtical stem segments believed to mainfest soil creep. The widespread occurrence of trees with the latter type of deformati<·�: can be more validly related to mP�hanical and physiological causes .

Parizek, �. R. , 1969 , An environmental approach to land use in a folderl and faulted carbonate terrane , in Environmental planning and geology: Washington, DC, u.s. Department of Hous ing and U.S. Dept . of Interior, p. 122-143. Discusses environmental problems in Valley and Ridge karst areas .

Parizek, R. R. , 1976, on the nature and significance of fracture traces and lineaments in carbonate and othe r terranes, in Yevjevich, v. , ed ., Karst hydrology and wa' .!r resources : Proceedings of the U.S.-Yugoslavia Symposium, Dub•ovnik, June 2-7 , 1975: Ft. Collins , CO, Water Resources Publications, p. 47-108. Yield probability plots show that both lineament and nonlineament wells can be highly pro&uctive , particularly when they penetrate zones of fracture concentration revealed by fracture traces . However, lineament wells we re more consistent in yield a�d displayed less variability for the same setting.

Parizek, R. R. , White, w. 6. , and Langmui r, D. , 1971, Hyd rology and geochemistry of folded and faulted carbonate rocks of the Central Appalachian type and related land use problems: Pennsylvania State University, Earth and Mineral Sciences Experiment Station , Circular , v. 82 , 183 p. Of particular interest are Part lB , Hydrogeologic framework of folded and faulted carbonates , and Part 4, Land use problems in carbonate terranes . Part lB considers interaction among stratigraphy, topography, and structure , as well as effect of fracture traces.

Parker, B. c., Wolfe, H. E., and Howa rd, R. v. , 1975, On the origin ar.i history of Mountain Lake , Virginia: Southeastern Geology, v. 16, p. 213-226 . Suggest origin of Mountain lake was by damming of stream head waters by colluvium. The extreme fluctuations in the lake level , borne out both by microfossil assemblages and ob�ervations in recorded history, are explainable by an incomplete damming to the present . Fig. 3 shows historical chronology of wate r level in lake .

Parker, J. M. , III, 1946, Residual kaolin deposits of the Spruce Pine district, North Carc.lina: North Carolina Division of Mineral Resources Bulletin, v. 48, 45 p. All the known deposits occur where the granite bodies unde rlie the strath of the North and South Toe Rivers and their tributaries. Pl. 4 shows limit of commercially important kaolinization as related to geology and topography.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Patton, J. B., 1956, Earth slips in the Allegheny Platea1.1 region: Journal of Soil and Water Conservation, v. 11, p. 28-31 , 33. Conditions leading to slips are 1) soil with a clayey, slowly permeable lower subsoil, formed on smooth clay shale andjor shale · and siltstone ; 2) a fairly steep, unstable slope ; 3) excessive surface and subsurface water. Slips are most common on native grass pastures.

Patton, P. C., a, d Baker, v. R., 1976 , Morphow�try and floods in small drainage basins subject to diverse hydrogeomorphi c controls: Water Resources Research, v. 12, p. 941-952. Discusses morphometry of drainage basins (as d�termined from stereo pairs) as a predictor of floods. Appalachians is only one of many areas studied. Notes that morphometric parameters for low-potential flash-flood areas (Indiana and Appalachian Plateau ) are better estimators of frequent low-magnitude runoff events (mean annual flood), while the same parameters corielate better with the maxi� flood of record in high-flood potential regions .

Pavich, M. J., 1974, A study of saprolite buried beneath the Atlantic Coastal Plain in South carolina [Ph.D. thesis] : Baltimore, Johns Hopkins, 214 p. Continuous cores of saprolite from beneath Coastal Plain sediments 25 miles southeast of the Fall Line �� re subjected to mineralogical and chemical analysis. These analyses and hydrochernic31 studies of the aquifer� which occur above and below the saprolite lead to the conclusion ·.:fiat the saprolite was formed prior to Cretaceous TUscaloosa sedimentation and that it has not been diagenetically altered in the subsurfac� . The saprolite therefore provides information about chemical weathering of crystalline basement prior to TUscaloosa time. Seismic and drilling data incicate that the buried crystalline surface is more planar than thf! presently exposed Piedmont surface, having a maximum relief of about 40 ft .

Pavich, M. J. , 1985, Appalachian piedmont morphogenesis: Weathering, erosion, and Cenozoic uplift, in Morisawa , M. , and Hack , J. T. , eds. , Tectonic geomorphology: Proceedings of the l�th Annual Binghamton Geomorphology Symposium, September, 1984: Boston, Allen & Urtwin, p. 299-319. Compares rates of uplift, weathering, and erosion; the mean rates are within a factor of two . Argues that : 1)long-terrn ongoing processes have determined the landforms and regolith distribution on the Appalachian Piedmont; and 2) isostatic compensation for mass lost by weathering and erosion has been a major component of continued uplift of the Piedmont throughout the Cenozoic. A methodology is proposed for obtaining data from the weathering profiles and rocks of the Piedmont to directly test the areal variation of uplift and erosion rates Li rough the late Cenozoic.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pavich, M. J. , 1986, Processes and rates of saprolite production and erosion on a foliated granitic rock of the Virginia Piedmont , in Colman , s. M. , and Dethier, D. P., eds. , Rates of chemical weathering of rocks and minerals: New York, Academic Press, p. 551-590 . Chemical considerations indicate that mass loss in solution during the formation of saprolite is most limited by availability and rate of movement of water. Calculates that 1mof saprolite is produced in about 250,000 yr. This rate is matched by the appa rent rate of local Piedmont s,1rface lowering since the late Miocene . Th inks V- snaped stream \alleys in Piedmont do not necessarily indicate recent downcutting .

Pavich, M. J. , Brown, L. , Klein, J. , and Middleton, R. , 1984, Berylliurn-10 accumulation in a soil chronosequence : Earth and Planetary Science Letters, v. 68, p. 198-204. Measured the concentration of the cosmogenic isotope Berylliurn-10 in soil samples from various horizons from 5 Coastal �lain and 1 Piedmont site whose ages are approximately known. overall, data indicate that Be-10 accumulation could be used to assign ages to soils if Be is not �bilized and lost from the soil profile .

Pavich, M. J., Brown, L. , Valette-Silver, J. N. , Klein, J. , and Middleton , R. , 1985, lOBe analysis of a Quaternary weathering profile in the Virginia Piedmont : Geology, v. 13, p. 39-41. Despite uncertainties about the processes by which Berylliurn-10 may be intercepted before entering the solurn and eroded after incorporation, a minimum age may be calculated for the regolith. This calculation is based on the delivery rate of lOBe and its decay rate and suggests that this residual profile developed during a period no shorter than 800,000 yr . The calculated minimum age may be within a factor of 2 of maxinrurn-age estimates based on surface lowering by erosion and on the rate of rock weathering to saprolite.

Pavich, M. J., and Markewich, H. w. , 1979, Soil stratigraphy of fluvial terraces along the Potomac and Rappahannock rivers, Virginia [Abstract): Geological Society of America Abstracts with Programs, v. 11, p. 207. Most prominent terraces along Rappahannock and Potomac rivers are at 3-6 m, 12-18 m, and 27-36 m. Soils formed on successively older terraces have a greater thickness of the A+B horizon, and have B horizons that increase in thickness, in percent clay, and in the ratio of crystalline to amorphous iron. The terraces range in age ftom late Pliocene to late Pleistocene .

Pavich, M. J., and Obermeier, s. F., 1985, Saprolite formation beneath Coastal Plain sediments near Washington , D.C. : Geological Society of America Bulletin, v. 96, p. 886-900. Three lines of evidence indicate that the saprolite formed in the subsurface and is post-Miocene in age : 1) thickness is thicker beneath sands and thinner beneath clays , apparently a function of the permeability of the ove rlying material ; 2) no evidence of soil formation at the upper surface of the profile; 3) consolidation tests indicate ove rconsolidation resulting from a thicker pre-Upper Miocene overburden . Hence , not all saprolite beneath Cretaceous sediment is pre-Cretaceous in age .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Peltier, L. c. , 1945, Block fields in Pennsylvania [Abstract) : Geological Society of America Bulletin, v. 56 , p. 1190. Notes that one block field overlies Illinoian till and suggests that the block fields reflect a periglacial climate of Wisconsin age .

Peltier, L. C. , 1949, Pleistocene terraces of the Susquehanna River, Pennsylvania: Pennsylvania Geological Survey , 4th Series, Bulletin, v. G2 3, 151 p. Discusses correlat1on of Pleistocene outwash terraces, giving detailed descriptions of pebble weathering. Describes two ages of

"congeliturbation" ma�.. rial (i.e., colluvium) . On p. 73, reports a statistical analysis 50 boulders in a blockfield - no preferred orientation was found . Peltier attributed the lack of orientation to subsidence that occurred when the fine interstitial material was washed out. Block fields marked on sketch map.

Peltier, L. C., 1950, The geographic cycle in periglacial regions as it is related to climatic geomorphology: Association of American Geographers Annals, v. 40, p. 214-236 . Briefly mentions Appalachians . Notes that in the periglacial cycle, 3 coexisting types of erosion surfaces develop: a surface of denudation produced by congeliturbation, a surface of lateral �lanation produced by the concentrated action of congelifluction wherever the water table and the zone of frec;t.:�nt freezing and thawing coincide, and stream-graded surfaces, frequently aggraded.

Peltier, L. C. , 1959. Late Pleistocene deposits [in Willard, B., Geology and Mineral Resources of Bucks County, Pennsylvania ): Pennsylvania Geological Survey Bulletin, v. C9 , p. 163-184. Discusses Pleistocene terraces of Delaware River, plus periglacial deposits.

Pe rkins, C. H. , 1870, Notice of a recent landslide on Mount Passaconaway : American Journal of Science , v. 49, p. 158-161 . An early description of a landslide , apparently a debris avalanche , in NewHamps hire.

Pe rry, W. J., Jr. , and Colton, G. W. , 1981 , A s\llllllary of the methodology and results of regional joint-studies in the central and northern Appalachi&n basin conducted by the U.S. Geological Survey as a result of Department of Energy Interagency Ag reement #EX-76-c-01-2287 : u.s. Geological Survey Open-File Report, v. 81-1341, 16 p. Purpose was to determdne if the trend of surface joints in younger rocks could be a reliable key to joint trends in the Devonian sr4les at depth. Concluded no , because the rocks of different lithologies generally exhibited different patterns of joints and different spacing of joints, at least partly as a function ,,f weathering.

Petty, J. J., 1932, Pedestal rocks of granite in the southern Piedmont: Journal of the Elisha Mitchell Scientific Society, v. 48, p. 119-122. Describes and provides 2 good photos of pedestal rocks in the Carolinas. Says due largely to chemical weathering that acts at or near the soil surface on projecting rock masses .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pewe , T. L. , 19&3, The periglacial environment in North America during Wisconsin time, in Porter, S. C. , ed ., Late-Quaternary envi ronments of the United States: The Late Pleistocene : Minneapolis, u. of Minnesota Press, p. 157- 189 . Table 9-2 lirts localities of ice-wedge casts, some of which are in New England . Fig. 9-11 shows periglacial features of Wisconsin age in the contiguous u.s. Table 9-7 lists localities of Wisconsin-age periglacial features in the eastern u.s.

Philbrick, S. s. , 1962, Old landslides in the uppe r Ohio Valley [Abstract ): Geological Society of America Special Paper, v. 68, p. 245-246 . Carbon-14 dates of wood from slide planes at Hildebrand Lock and Dam, 4 miles southwest of Morgantown, wv, and Pike Island Locks, 6 miles north of Wheeling, WV, are respectively 8940 plus or minus 350 yr and 9750 plus or minus 200 yr .

Phipps, R. L., 1974, The soil creep-curved tree fallacy: Journal of Research of the u.s. Geological Survey, v. 2, p. 371-377. Notes that no evidence has been found in eastern deciduous forests to substantiate statements that curved tree trunks, downslope tilted tree trunks, and upslope trailing tree roots are the result of soil creep.

Pickering, S. M., Jr., and Higgins, M. w. , 1979, Georgia from space - an explanation of the NASA Landsat 1 satellite image color mosaic of the state of Georgia: u.s. Geological Survey Circular, v. 787 , 21 p. Pages 5-14 illustrate Georgia landforms.

Pierce , K. L. , 1965, Geomorphic significance of a Cretaceous deposit in the Great Valley of southern Pennsylvania: u.s. Geological Survey Professional Paper, v. 525-C, p. Cl52-cl56 . A lignitic terrestrial deposit of Late Cretaceous age {as identified by plant macrofossils) appears to rest on more than 170 ft of residuum from carbonate rocks. After accumulation, probably in a sink , this deposit may have been lowered hundreds of feet by solution of the underlying carbonate rocks. Erosion totals for this and other areas were calculated on the basis of thickness of residuum and insoluble content of the bedrock . All these estimates indicate an average erosion of the Appalachians of at least several thousand feet since deposition of the lignite .

Pierce , K. L. , 1966, Bedrock and surficial geology of the McConnellsburg quadrangle, Pennsylvania: Pennsylvania Topographic and Geologic Survey Atlas, v. 109a, 111 p. Mapped surficial deposits in unglaciated Valley and Ridge . 7 map units. Basic division is into residua� vs . transported regolith. Discusses scree , block fielas, rubble, rubble ridges, fan-shaped diamicton deposits, roundstone diamicton. Subjected latter to grain-size, roundness, lithologic, and fabric analysis. Thinks roundstone diamicton is deeply weathered alluvial gravels. Also discusses topographic surfaces and bedrock control of landscape .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pitman , w. c. , III, and Golovchenko, X. , 1979, The role of sea level change in the shaping of the Appa lachian Mountains : ��L-Donerty Geological Observatory Yearbook , v. 6, p. 31-34. Reconstructed Schooley peneplain for area N of Harrisburg and calculated the amount of isostatic subsidence this �uld cause - 240 m. Peneplain, of course , was probably near sea level when formed. Sea level was probably near present level early in the late CretJceous , then slowly rose for about 40 m.y. Some time in the later Early Cretaceous sea level had risen to about 240 m above present and the Appalachians had been eroded near sea level . Sea level continued to rise, howeve r, depositing as much as 275 m of sediments on the peneplain (calculated from expected subsidence as sea rose to peak of 350 m above present ). As sea level subsequently fell in Late Cretaceous , streams were supe rimposed and coastal plain sediments re100ved . Authors thus suggest that Johnson may have been right .

Plaster, R. w., and She��. w. C. , 1971, Bedrock weathering and residual soil formation in central Vi rginia: Geological Society of America Bulletin, v. 82 , p. 2813-2826 . Compared soils developed on limestone , hornblende metagabbro, and granitic gneiss. Concluded that when other factors are not greatly different, the bedrock plays a very important role in determining the cha racteristic properties of the overlying soil profile .

Pomeroy, J. S., 1977, Landslide susceptibility map of th� Pittsburg west quadrangle , Allegheny County, Pennsylvania [Map]: U.S. Geological Survey Miscellaneous Investigations Series, v. I-1035, 1 p. Mapunits include recent landslides, prehistoric landslides, slopes with IOOderate to severe susceptibility to landsliding , slopes with slight to IOOderate susceptibility, steep slopes 100st susceptible to rockfall, and ground with little susceptibility to landsliding. Scale 1:24,000 .

Pome roy, J. S., 1978, Isopleth map of landsljde deposits, Washington County , Pennsylvania - a guide to compara�ive slope stability: u.s. Geological Survey Miscellaneous Field Studies, v. MF-1010, 2 p. Isopleth ma? shows the percent of area covered by landslide deposits: 70-80+ percent, very high to severe susceptibility to landslides; 50-70, high to very high; 30-50, IOOderate to high; 10-30, low to moderate ; 0-10, nil to low. Scale 1:50,000 .

Pomeroy, J. S., 1980, Storm-induced debris avalanching and related phenomena in the Johnstown area, Pennsylvania, with reference to other studies in the Appalachians : U.S. Geological Survey Professional Paper, v. 1191, 24 p. Only a small percentage of debris avalanches has taken place along well-defined hollows. Most ll"OVement is rather along planar to gently concave slopes, which may or may not be part of a wider, laterally concave slope . unlike debris av. causing a chute , IOOVement of debris from nonchanneled debris avalanches ceases downslope wherever a lessening of grade reduces the velocity of 100vement and causes a pileup of �a terial.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pome roy, J. s. , 1982, Geomorphic effects of the July 19-20, 1977, storm in a part of the Little Conemaugh River area northeast of Johnstown, Pennsylvania: Northeast Geology, v. 4, p. 1-9 . Storm dumped �0 em of rain in 9 hr. Debris avalanches weremost conspicuous features . Less obvious but more nume rous slumps took place along more moderate slopes. The combination of steep slopes and thick colluvium unde rlain mostly by rocks of the Allegheny Group accounted for much of the mass movement. Approximately 75 percent of slides took place in the NW to NE quadrant . Largest amount of erosion was accomplished by stream-channel enlargement.

Pome roy, J. s. , 1982, Landslides in the greater Pittsburg region, Pennsylvania: u.s. Geological SUrvey Professional Paper, v. 1229, 48 p. Describes landslides using stereo aerial photJs and pieces of 1:24,000-scale maps . Notes that an aerial photo of 1:12, 000 or larger is necessary for detailed lar�slide studies in urban areas.

Pomeroy, J. S. , 1982, Mass movew2nt in two selected areas of western Washingtcn Com1ty, Pennsylvania: u.s. Geological Survey Professional Paper, v. 1170-B, 17 p. The earthflow is the dominant landslide type in the Dunkard terrain of the Short Creek area and is caused largely by natural forces. More than 75 percent of the recent slides took place on � to E-facing colluvial slopes because of the combination of steeper slopes and greater soil moisture .

Pomeroy, J. s., 1983, Relict debris flows in no• thwestern Pennsylvania : Northeastern Geology, v. 5, p. 1-7 . Large relict colluv

Pomeroy, J. S. , 1984, Sto�induce1 slope movements at East Brady, northwestern Pennsylvania: u.s. Geological Survey Bulletin, v. 1618, 16 p. Almost all the debris avalanching took place along existing hillside depressions. The bedrock-colluvium contact served as Lle slippage surface for most of the 1980-storm slope movements . Slope movement involving beth colluvium and bedrock has been continual throug,,vut historic and prehistoric time. Fig. 12 is schematic diagram showing colluvial slope movements along concave slopes or hollows and above benches. Fig. 13 is cross section showing recc.1t and relict shear surfaces .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Pomeroy, J. 5. , and Thomas , R. E. , 1985, c� ologic relationships of slope movements in nc tthen. Alabama : U.S. Geological Survey Bulletin, v. 1649, 13 p. In the CUmberland Plateau , slopes underlain by the Pennington Formation ana;or the Bangor Limestone are the most susceptible to movement. Toppling failures, involving the subho�izontal ove rlying Pottsville Formation, are largely controlled by separation along the ve rtical joint faces and by undermining. Slopes unde rlain by the Pride Mountain Formation in the Highland Rim section show evidence of present and past instability.

Potter , N. , Jr., 1985, Colluvial and alluvial gravels, carbonat� weathering and preservation of a Cenozoic erosional history in the Great Val ley, southeastern Pennsylvania [Abstract ]: Geological Society of America Abstracts with Programs, v. 17 , p. 59 . Alluv ial depos its on the valley floor are markedly different on the two major rock types there . On the SE side, thick alluvial fans of quartzite cover residuum from deeply weathered carbonate rocks for distances of 2-4 km from the mountain front . The coarse gravels inhibit fluvial removal of residual clays , allowing the clays to accumulate for long periods of time. Solution of the underlying carbonates apparently traps the gravels. On the NW side o: the valley, shale is the dominant bedrock , and gravels extend only a short distance from the mountain front . Patches of gravel are common , however, usually as a veneer of pebbles and cobbles of quartizite on shale uplands along major stream courses, up to 30 rn above the modern stream.

Potter, N., Jr. , and Moss, J. H. , 1S68, O'"� gin of the Blue Rocks block field and adjacent deposits, Berks County , Pe�1sylvania: Geological Society of America Bulletin, v. 79, p. 255-262. Blue Rocks block field is about 0.5 mi long and is composed of Tuscarora blocks. Tabular blocks in the block field 11ave an imbricate structure and describe a series of lobes in which the blocks dip strongly upslope . The blocks are crudely sorted vertically, with coarser material at the surface. Blue rocks and the adjacent rubble closely resemble solifluction sheets or terraces on the Seward Peninsula. the lack of fine material probably resulted in part from the flushing of fines after downslope movement ceased .

Potter , P. E. , 1955, The petrology and origin of the Lafayette gravel , pt . 2: Geomorphic history: Journal of Geology, v. 63, p. 115-132 . The heavy-mineral and feldspar content establishes the preglacial age of the Lafayette . Physiographic evidence indicates a Pliocene age . Epeirogenic uplift rather than late Te rtiary climatic change or eustasy is believed to have initiated gravel deposition . Alluvial fan deposits at the head of the Mississippi embayment wer� favored by phys iographic position. The location and magnitude of the fans in pa�t controlled the entrenchment posiLions of the Tennessee, Mississippi , and Cumberland-Ohio rivers.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Powell, R. L. , 1Q�3, Alluv iated cave springs of south-central Indiana : Indiana Academy of S�iences Proceedings , 1962, v. 72, p. 182-189. Descrilx·s 7 artesian springs that are actually alluviated cave springs - cave springs that have been buried by accumulations of alluvial sediment in a previously deeper valley.

Powell, R. L. , 1964, Origir of the Mitchell Plain in south-central Indiana : Indiana Academy of Sciences Proceeding , 1963, v. 73, p. 177-182 . Discusses origin of the Mitchell Plain, a karst plain that has formed by solution of a thick series of limestones of middle Mississippian age .

Powell , R. L. , 1966, Groundwater movement and cavern development in the Chester Series in Indiana : Indiana Academy of Sciences proceedings , 1965, v. 75 , p. 210-215. The features of the known cavetns in these rocks indicate the direction and amount of groundwater movement within the caverns and the ove rlying strata .

Powell, R L. , 1968, The geology and geomorphology of Wyandotte cave , Crawford County, Indiana : Indiana Academy of Sciences Proc�edings, 1967, v. 77, p. 236-244. Wyandotte Cave is unique among cave rns in the Crawford Upland mainly becaus� of the clarity with which its stratigraphic position and geomorphic history may be interpreted . • has developed along joints in the bedrock , more or less along the dip of the strata , as a subterranean tributary to Blue River. Three major cavern levels lie at grade with three erosion levels along Blue River, indicating that the different levels range in age from Tertiary to middle Pleistocene . Each level , however, has its peculiarities, depending upon differences in lithology which markedly control the shape of the original solution passages and the mechanics of cavern collapse .

Powell, R. L. , 1970, Geology of the Falls ol the Ohio River: Indiana Geological Survey Circular, v. 10, 45 p. Includes discussion of the geomorphology of the falls. Fig. 7 consists of 3 block diagrams showing the progressive development of the falls.

Powell, R. L. , 1977 , Lateral unloading of isotrc�ic rock as a process of solution channel enlargement , in TOlson, J. s. , and Doyle , F. L. , eds. , International Association of Hydrogeologists Memoir 12 [Karst hyd rogeology] : Huntsville, AL, tJniv. Alabama at Huntsv.i.lle, p. 433-441 . Some subterranean conduits in isotropic carbonate strata may be formed principally t.y exfoliation. Passages formed by this pro cess commonly have a circular cross section, except where modified by subsequent solution and failure of wall and ceiling rock . The diameter of the passage is essentially equal to the thickness of the isotropic stratum. The passage develops initially by solutional enlargement alon� a joint, followed by pressure-release jointing which allows rock parallel to the two joint faces to unload into the na rrow cavity as thin sheets and spalls, which are then ren10ved . The rock types known to be thus affected are gene rally fine-grained friable dolostones and calcarenites .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Powell, R. L., and Thor� -y, W. D. , 1967 , Ka rst geomorphology of south-central Indiana , in SchneidE A. F. , ed ., Geologic tales along Hoosier trails: Field tr:.p guide for N-C section of the GSA, Indiana University, April 19- 22 , 1967 : Bloomington , IN, Indiana Geological Survey, p. 11-37 . Mainly a road log . �tops i�clude Twin Caves , Tolliver swallow hole , Wesley Chapel gulf, karst valley of Dry Bran�h, the Orangeville rise, Radclif.f Springs overlook , and Marengo Cave .

Powell, w. J. , and LaMoreaux , P. E. , 1969, A problem of subsidence in a limestone terrane at Columbiana , Alabama: Alabama Geological Survey Circular, v. 56 , 30 p. Most of the subsidence was confined to the material above the limestone in a zone consisting of cl�y, shale, slate , sand , and gravel, and occurred in an area adjacent to the trace of the Wi lsonville fault. Removal of silt, sand , calcareous and colloidal material by ground-water movement reduced the bearing strength of the overlying material. Suggestions are presented for alleviating future subsidence .

Prowell , U. C., and O'Connor, B. J. , 1978, Belair fault zone - evidence of Tertiary fault displacement in eastern Georgia: Geology, v. 6, p. 681-684. The Belair fault zone is a series of northeast-trending obl ique-slip reverse faults that cut the inner margin of the Coastal Plain near Augusta . The zone has had as much as 30 m of apparent vertical offset since the deposition of the Late Cretaceous to middle Te rtiary Coastal Plain sedimentary rocks. underlying crystalline rocks also are exposed.

Prowell , D. C. , O'Connor, 8. . , and Rubin, M. , 1976, Preliminary evidence for Holocene movement along Jhe Belair fault zone near Augusta, Georgia: u.s. Geological Survey Open-f1le Report, v. 75-680, 8 p. A trench cut across one of the faults in the zone shows lenses of organic material cut by and dragged into the fault. Radiocarbon dates indicate that this organic material is younger than 2500 yr.

Psilovikos, A. , and Var�outen, F. B., 1982, Ringing rocks barren hlock fie!d, east-central Penn�ylvania: Geology, v. 32 , p. 233-243. Blocks from diabase sill. Three distincti· e features characterize the bare blocks, vs . those in surrounding wood� ..nds : 1) random scattering of sizes and shapes; 2) conspi�ous shattering along joints; 3) solution pits on joint faces. Orientation of long axes is random.

Quinlan, J. F. , and EWers, R. 0. , 1981 , Hydrogeology of the Manlnoth cave region, Kentucky, in Roberts, T. G. , ed ., GSA Cinc] nnati 1981 fie:� trip guidebooks: geomorphology, hydrogeology, �eoarcheology, engineering geology: Falls Church, VA, AGI , p. 457-506 . Discusses delineation of Mammoth Cave region groundwater basin by means of dye tracing, cave mapping, and construction of potentiometric maps . Total of 34 stops , concerning all aspects nf karst and karst hyd rogeology.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Quinlan, J. F., and Ewers, R. 0. , 1985, Ground water fl'JW in .imestone terr.mes : Strategy, rationale, and procedure for reliable, �fficient monitoring of ground water quality in karst areas, in Proceedjngs of the Fifth National Sympc sium on Aquifer Restcration and Ground Wa ter Monitoring: Worthington, OH, National Water Well Association, p. 197-234 . The probability of a randomly-drilled monitoring .... -ell intercepting the trunk conduit that drains a ground water basin is similar �o the probability of a dart randomly thrown a... a wa ll map of the u.::;. hitting the Mississippi River. Therefore, springs - rather than wells - are the most logical places to monitoring for pollutants in limestone terranes . Describes proper development of such a monitoring network . Fig. 3 - excellent block d�agram showing conduit and diffuse flow in a maturely karsted aquifer.

Quinlan, J. F., and EWers, R. 0. , 1986, Ground water flow in the Ma!mnoth Cave area, Kentucky, with emphasis on priuciples, contaminant dispersal , instnnnentation for monitoring water quality, and other methods of study , ir. Envi ronmental problems in karst terranes and their so' utions : Field trips : Worthington, OH, National Water Well Association, 93 p. Thisguide book is an updated, partially edited reprint of part of a guidebook first published in 1983 by the Indiana Geological Survey. Includes Quinlan and Ewers' ( 1985) NWWA paper. Covers determination of ground water basins and cave geomorphology, as well as monitoring principles.

Quinlan, J. F., and Pohl , E. R., 1967, Ve rtical shafts a�tively promote slope retreat and dissection of the solucion escarpment and the Chester cuesta in the Central Kentucky Karst [Abstract): NSS Bulletin, v. 29 , 109 p. Along the Chester Cuesta, in a zone generally no wider than 200 ft, vertical shafts number 200 to 500 per linear mile of caprock outcrop. Interstratal karstification at the sandstone-limestone contact has differentially lowereG both large and small masses of caprock . The detritus may either collapse catastrophically into the vertical shafts or it may subside concomi tantly wi�, solution.

Quinlan, J. F., and Rowe , D. R. , 1977, Hydrology and wa ter quality in the Central Kentucky Karst: University of Kentucky Water Resourc< Research Institute Research Report, v. 101, 89 p. Traced heavy-metal-rich effluent from a wastewater treatment pl��t . Dye tracing and cave mapping allowed groundwater basins to be delineateo .

Quinlan, J. F., and Rowe , D. R. , 1977, Review of the physical hydrology of the central Kentuck�{ Karst, in Dilamarter, R. R. , and Csallany, S. c., eds., Hydrologic problems in karst re�ions : Bowling Green, KY,Western Kentucky Universit�·, p. 50-63. The Pennyroyal Plateau cunsists of the Sinkhole Plain and the Glasgow Upland . The s�nkhole Plain is flanked on the north by the sandstone-capped Chester Escarpment and Chester Cuesta. Dye tracing and cave �pping have allowed 13 groundwater basins to be delineated; all but 2 of them are characterized by distributary complexes 50 m to 4 km wide which diGcharge at one or several springs at each of 2 to 14 loc�tions .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Quinlan, J. F. , and Rowe , D. R. , 1978 , Hydrology and water quality in the Central Kentucky Karst: �hase II Part A: Preliminary summary of the hydrogeology of the Mill Hol& sub-basin of the Turnhole Spring groundwater basin: University of Kentucky Wa ter Resources Research Institute Research Report 109, 42 p. Water from upland areaE flows to small ephemeral and perennial springs that feed sinking streams that are tributary to low-order cave streams. These cave streams , also recharged by diffuse percolation, are part of a dendritic network in which intermediate-oLder streams join high-order streams that flow to major trunk streams . The location of the latter can be inferred from the position and orientation of well-defined troughs in the piezometric surface . Flow routes within the Parker cave system are highly varia�le and determined by changes in flood stage .

Quinlan, J. F., and Rowe , D. R. , 1981, Groundwater basins in the Mammoth Cave region, Kentucky [Map) (�casional Publication 1): Mammoth Cave , KY, Friends of the Ka rst, 1 p. Four-color, 1:138, 0[0-scale map showing springs, major caves, flow routes, and potenti�tric surface of Mammoth Cave region.

Radbruch-Hall, D. H., Colto� . �. B., Davis, w. E. , Skipp, B. A. , Lucchitta, I., and Va rnes, D. J. , 1982, �slide ove rview map of the conterminous United States: U.S. Geologj cal uurvey Professional Paper, v. 1183, 25 p. Mapwith scaie of 1:7,500,000 shows low, uoderate, and high susr�ptibilty, and low, moderate, and high incidence of landsliding in tHe U.S. Much of Pla::..aau and Blue Ridge provinces are in high incidence category. In the Appalachians , earth flows , debris flr s, and debris avalan�hes predominate in weathered bedrock and colluvium. Damaging debris avalanches result when persistent steady rainfall is foll�� by a sudden heavy downpour Landsliding in unweathel� Dedrock is controlled locally by joint systems . In some places . outward gravitational movement of valley walls due to stress relr ·sf' has formed anticlines and caused thrusting in the center �1 valleys .

Rader, E. K. , Gathright, T. '•· • "!ilici , R. c. , Schultz, A. P. , Conley, J. F. , Evans, N. H. , and Venk :' 'krtshnan , R. , 1987, Structural geology from the Appalachian Plateau t0 .,,e :nner Piedmont of Vi rginia, in Geological Society of America Sout.J.�c.stern Section, Field Trip Guidebook, Field Trip 1: NOrfolk, Old Dominion University, p. 1-41. Stops 2 and 3, p. 15-18, describe giant rockslides on the flanks of Sinking Creek Mount.a' ::.

Rai sz , I., and Henry, J., i9 '., . An ave rage slope map of New England : Geographical P.eview, v. ;;7 , p. 467-472. Slope-map categorit•i' . in ave rage feet/mile: 50, 100, 200, 300 , 400 , 500+ .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Rapp, A. , 19�7, Pleistocene activity and Holocene stability of hillslopes with examples from Sca�dinavia and Pennsylvania, in L'evolution des versants (Les Congres et Colloques de l'Universite de Liege , v. 40): Liege , France, Universite de Liege , p. 229-244. Says that in Pennsylvania, the survival of sorted boulder stripes, sorted polygons, block fields, soliflucti Jr. beds, and stabilitzed talus slopes tPstifies to the ineffectiveness of contempora"Y slope processes . Notes tree roots may have disturbed many sorted polygons. Describes examples of the above-mentioned features in Pennsylvania.

Rasmussen, w. c. , 1953, Periglacial frost-thaw basins in New Jersey: A discussion: Journal of Geology, v. 61, p. 473-474. Discusses Wolfe 's (1973) article in same journal . Says that any comprehensive theory of the formation of the basins must either account for their wide geographic distribution on the Atlantic Coastal Plain or show that somewhere along their spread the basins change in character or in origin.

Rauch , H. , 1974, ThE �ffects of silty streaks and bedding partings on c�{e

developnent in � "1tral Pennsylvania, in Rauch, H. W. , and Eberhard, E. , eds., Fourth conference on karst geology and hydrology, p�oceedings : Mo rgantown, WV, WV Geological and Economic Survey, p. 153-160 . Cave developnent increases with the increasing abundance of small silty streaks, due largely to the increased surface area of rock exposed to dissolution along the bedding partings. Howeve r, silty streaks over about 5 mm in thickness are associated with fewer minor solutional features and generally with less cave development . This is probably because of decreased infiltration rates for ground water and decreased area of pure carbonate rock exposed along associated bedding fractures. Major bedding partings are localized along thick silty streaks and shale layers. cave development generally increases as the spacing of major bedding partings increases.

Rauch, H. W. , 1972, The effects of lithology and other hydrogeologic factors on the development of solution porosity in the middle Ordovician carbonates of central Pennsylvania [Ph.D. thesis) : University Park , PA , Pennsylvania State University, 547 p. Solution rate and cave volume decrease with in�reasing doloaUte, for dolomite contents above 14 percent . Impurities such as clay, quartz , feldspar, and insoluble opaques act to decrease the solubility rate and cave development . An increase in the abundance of silty streaks, however, generally increases the solubility rate . Major bedding partings usually aid cave development by promoting ceiling breakdown. cave volume generally increases as spacing between major bedding partings increases . caves near ridges generally become more frequent but smaller near wa ter gaps . Cave size generally increases with decreasing stratigraphic dip.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Raup , H. M. , 1951, Vegetation and cryoplanation [From symposium: The glacial border - climatic, soil, and biotic features] : Ohio Journal of Science , v. 51 , p. 105-116. Tentatively concludes that the present local distribution of red oak and white ash in Harvard forest was determi.ned by the re.,.'Orking of glacial and wind-blown soils that occurred during the period of in�tability after the retreat of the last ice . This is done by determining the thickness of loamy solifluction debris at a given site.

Ray , L. L. , 1963, Quaternary events along the ung1aciated lower Ohio River valley: U.S. Geological Survey Professional Paper, v. 475-B, p. B125-B128 . Tills that are far more deeply weathered than those of the Illinoian glaciation are exposed within the valley of the Ohio and south of the river above Louisville . The alluvial history of the Ohio River valley below Louisville was intimately aff�cted by glaciers invading its drainage basin. Alluviation of a deep bedrock valley and the lower courses of tributary streams is interpreted partly from the stratigraphy of loess deposits genetically related to valley trains .

Ray, L . L., 1965, Geomorphology and Quate rnary geology of the Owensboro quadrangle, Indiana and Kentucky: U.S. Geolog1cal Survey Professional Paper, v. 488, 72 p. Successive surfaces of erosion of Pliocene age are represented along th·� ancient Ohio by a series of high-level gravel deposits resting on bedrock benches above the level of the present river. Interprecs these to be the result of intermittent , possibly differential regional uplift of Pliocene age . In OWensboro quad there is evidence for the last three of these erosional stages. During each invasion of contin�.1tal ice sheets, a valley train was produced in the area. Because aggradation during glaciations exceeded interglacial degradation, alluvium has gradually filled the preglacial bedrock valley to a maximum depth of 200 ft. Describes oldest deposits of area. Color surficial geology map of quadrangle accompanies report.

Ray , L. L. , 1966, Pre�isconsin glacial deposits in northern Kentucky : u.s. Geological Survey Professional Paper, v. 550-B, p. B91-B94 . Three tills of pre�isconsin age . The oldest, whic!1 Ray called the Nebraskan, is most widespread and most deeply weathered, and occurs on remnants of a preglacial upland . Till of what he calls Kansan age is less widespread and less deeply weathered, and ove rlies the Nebraskan till on the upland near Cincinnati , and is present elsewhere at subsummit positions in valleys cut in the glaciated upland during Aftonian time. The youngest till, the Illinoian, is present at a few places within the Ohio valley and on the adjacent hills southeast of Cincinnati .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ray, L. L., 1969, Glacial erratics and the problem of glaciatior. in northeast Kentucky and southeast Ohio - a review and suggestion: U.�. Geological Survey Professional Paper, v. 650-D, p. Dl95-Dl99. In order to explain erratics in NE Kentucky and SE Ohio, Ray suggest� that a glacial advance , possibly of Nebraskan age , P.·cended somewhat beyond the mapped limits of glaciation in southern and southeast Ohio and into northern Kentucky . Such an advance would provide for emplacement cf the glacial erratics through ice rafting. Describes two l�rge erratics beyond known range of glaciation.

Raymond , L. A. , 1977, Glacial , periglacial , and pseudo-glacial features in the Grandfather Mountain area, North Carolina : Southeastern Geology, v. 18, p. 213-229 . Periglacial features include tors, blockfields , blockstreams, stone lines, and a possible solifluction lobe . Probable relict glacial featues include cirques and a u-shaped valley.

Raymond, L. A. , 1979, We re Pleistocene glaciers present in the southeastern United States?, in Raymond , L. A. , ed., Second annual conference on the Quaternary history of the southeastern United States, proceedings , 1975: Boone , NC , Appalachian State university, p. 11-18. Evidence favoring glaciation in the southern Appalachians include 1) cirque-like features; 2) u-shaped valley on Grandfather Mt .; 3) paleotemperature studies that suggest a mean annual cooli�g of 15 to �0 degrees C during Pleistocene ; 4) paleontological st iies also suggesting much cooler conditions .

Raymond, L. A. , Cadwell , D. H. , and Haselton, G. M. , 1980, Further observations on glaciation in the Shining Rock area, North carolina: Discussion and reply: Southeastern Geology, v. 20, p. 165--173 . Raymond and Cadwell take Haselton to tack for reversing his earl�er opinion and reporting no evidence for alpine glaciation in the Shining Rock quadrangle . They show valley cross sections and longitudinal profiles that suggest a glaciated valley to them . Haselton notes that such profiles don't mean much .

Reed, J. C. , Jr ., 1964, Geology of the Linville Falls quadrangle , No rth Carolina: u.s. Geological Survey Professional Paper, v. 1161-B, p. 81-853. Pages 31-34 have brief but pithy discussion of alluvial fans, high-level gravels, c..nd flood-plain deposits. Notes that fan deposits commonly rest on saprolite derived from rocks similar to those which compose unweathered boulders in the fan , thus suggesting that some of the fans have been deposited subsequent to the formation of the underlying saprolite . No tes high-level gravels up to 150 ft above present flood plain; these terraces are discontinuous and exhibit no particular concordance in level . Are commonly overlain by a red clayey soil.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Reed , J. c. , Jr., 1981 , Disequilibrium profile of the Potomac River near Washington , D.C. - A result of lowered base level or Quaternary tectonics along the Fall Line?: Geology, v. 9, p. 445-450. Detailed study of the terraces along the Potomac in the Piedmont above Wa shington , D.C. , suggests that t� e discontinuity in profile at the Fall Line is the result of Quaternary downcutting in response to a lowered base level . Howeve r, in addition it is noted that the arrount of discrepancy at the Fiill Line between the actual profiles and the pr�jection of the profiles of the upstream reaches increases from about 27 m at the James River to about 50 m at the Susquehanna ; such a trend is consistent with a northward increase in uplift of the Piedmont . Thus, discontinuities at the Fall Line may be due in part to such uplift.

Reed , J. C., Jr., Bryant, B., and Hack , J. T. , 1963, Origin of some intermittent ponds on quartzite ridges in western North Carolina: Geologica,. Society of America Bulletin, v. 74, p. 1183-1187. several intermittent ponds and closed depressions as much as 200 ft wide occur on the crests of ridges in gently dipping Cambrian(?) quarzites in the southeastern foothills of the Blue �idge Mountains near Morganton. The unconsolidated fill and debris in the p<:>nds consists of materials that could have been derived completely from the quarzite. Depressions probably formed by solution during Quate rnary.

Reed , J. C., Jr., B�ant , B. , Jr., Leopold, E. B. , and We iler, L. , 1964 , A Pleistocene section at Leonard 's cut , Burke County, County: u.s. Geological Survey Professional Paper, v. 475-D, p. D38-D42. An exposure of peat described by Kerr in 1875 at Leonard's cut probably accumulated on a former flood plain of the Catawba River �11 below the Piedmont up1ar.d surface . Pollen assemblages and field relationships show that the deposit is nonglacial and probably represents an interglacial episode of the Pleistocne . Fig. 129.4 is a diagrammatic section of the deposits.

Reesman , A. L., and Godfrey, A. E., 1972, Ch�11J < ,1 erosion and denudation rates in Middle Tennessee: Tennessee Division t water Resources, Water Research Series, v. 4, 35 p. The topographic Central Basin is a breached domal structure that formed by differential chemical solution between the sili�eous Ft . Payne Formation (Mississippian) ard �e more soluble unde rlying

Ordovician limestones. Chemical dem· •, -. ::ates are about 10 .7 llllVlOOO yr for the Fort Payne and about .'· 5 llllVlOOO yr for the Ordovician limestones . Breaching and dev��upment of the Basin, from the first encounter with the ?ort �· yne , could have been accomplished by chemical erosion alone .n less than 10 m.y. Drainage evolution is also discussed.

Reesman , A. L., and Godfrey, A. E., 1981 , Dev .: �.opment of the Central Basin of Tennessee by chemical denudation : Zeitschrift fur Geomorphology, v. 25 , p. 437-456 . Similar to 1972 article by same two authors.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Reesman, A. L. , and Stearns , R. G. , 1985, EValuation of the Beech Grove linea�nt and factors controlling stream alignments in central Tennessee: Southeastern Geology, v. 26 , p. 1-19. The Beech Grove lineament, detected from Landsat imagery, comprises 9 separate stream valleys that form a remarkably straight 96-mi le-long feature trending N 21 E. The northern 21-mi reach may be tectonically controlled judging from its parallelism to gravity and magnetic anomalies, and proximity to mineralization. The central 38-mi reach is believed to result from superimposed straight streams originally controlled by the strike of cuestas , developed during the erosion of now removed Pennsylvani�n sandstones and shales .

Reesman , A. L., Walton, A. w. , Sprinkle , C. L. , Godfrey, A. E., and Srr�th, D. B. , 1975, Hydro-geochemistry in a carbonate basin - geomorphic and environmental implication: university of Tennessee Water Resourcec Research Center, Research Report 44, 265 p. A steady-state weathering model for Cartwright basin suggests that physical erosion is currently proceeding at rates of 5 to 10 times the steady state value . Denudation of pre-Fort Payne rocks ave rages about 170 ftjmy with the siliceous Fort Payne at about one third this rate (51 ftjmy) . Rapid denudation rates at cartwright result in part from concentratlons of pyrite in the rocks which produce 30+ ppm 504 and enhance carbonate dissolution.

Reinemund , J. A. , 1955, Geology of the Deep River coal field, North Carolina : u. s. Geological Survey Professional Paper, v. 246, 159 p. Pages 61-67 and 83-87 discuss su rficial deposits and geomorphol�;, including u�=o� levels of terracas .

Reinhardt, J. , and Cleaves, E. T. , 1978, Load structures at the sediment saprolite boundary, Fall Line, Maryland: Geological Society of America Bulletin, v. 89, p. 307-313. The response that the saprolite has made to the ove rlying lower Cretaceous sediments suggests that 1) the crystalline rock had weathered to saprolite before sediment emplacement ; 2) the sediment was deposited by a highly erosive agent; 3) the saprolite was water saturated and deformed plastically during sedimentation; 4) later reorientation of the sediment-saprolite deformation structures took place, probably during sedimentary compaction. Deformation took place in early Cretaceous time. Evidence seems to rule out 1) a Quaternary periglacial origin and 2) an origin involving saprolitization later than sedimentation.

Reinhardt, J. , Prowell, D. c. , and Christopher, R. A. , 1984, Evidence for Cenozoic tectonism in the southwest Georgia Piedmont : Geological Society of America Bulletin, v. 95, p. 1176-1187 . Paleocene nonmarine sediment in the Georgia Piedmont has been isolated from correlative Coastal Plain deposits by high-angle reverse faults and subsequent erosion . The reverse faults also offset surficial deposits of probable Pliocene age . The surficial deposits along the northern margin of Pine Mountain are notably more extensive than those in other regions of the Georgia Piedmont. The fan depos its have an erosional lower contact, are lP.nticular, and generally thin away from the base of the mountain.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Renner, G. T., 1927 , The phys iographic interpretation of the Fall Line : Geographical Review, v. 17, p. 278-286. The Fall Line occurs where there is a break in the slope of the land due to the intersection of the recently exposed margin of the tilted Jurassic(?) peneplain with the Te rtiary( ?) peneplain of the upla��s . The difference in slope of the two peneplains gives rise to a declivity in the course of near·.y every stream that crosses the line of intersection of the 2 peneplains. The re may be fall lines whe re no coastal plain exists

Renwi ck, W. H. , 1984 , Rates and processes of postglacial slope developnent near Ithaca , New York: Northeastern Geology, v. 6, p. 238-244. Fall Creek has incised through 2�-40 m of glacial s�iiments since about 12, 000 years ago , leaving a series of erosio�l terraces on the valley floor. The scarps of the terraces can be dated in relative terms by the elevation of the terraces at their base . The correlation c�fficient between heigh'- of base of slope above modern floodplain and ave rage slope is -.619; between height anc maximum slope angle, -.443. One ir.terpretation is that slope angles decline continuously through time (from 35-40 to 15-20 degrees ). More likely, however, slope profiles evolve rapidly upon cessation of basal erosion and thereafter change is slow or negligible .

Rhodehamel, E. C., and Carlston, C. W. , 1963, Geologic history of the Teays Valley in We st Virginia: Geological Society of America Bulletin, v. 74, p. 251-273. The segment of the abandoned Teays Valley between Scary and Huntingtor. stands 130-240 ft above the Ohio and Kanawha rivers. The bedrock floor is overlain by highly weathered gravel . As much as 100 ft of locally derived sediment ove rlies the basal gravel . Sand was deposited at each end of the valley but in the E-C part it grades laterally into a laminated sil�; clay that was deposited during a period of pending, probably in Kansan time . LOwer sediments resulted from later pending. Argues that Teays Valley was abandoned in preglacial times by normal stream-capture processes.

Rice, c. L. , 1981, Stream piracy ne ar Ivyton in eastern Kentucky, in Cobb , J. c., ed ., Coal and coal-bearing rocks of eastern Kentucky: Lexington , KY, Kentucky Geological Survey, p. 166-169. The capture of the headwaters of Burning Fork of Licking River by tributaries of the Big Sandy River is one of the best examples of s�ream piracy in eastern Kentucky. Tributaries of Middle Creek and Jennys Creek join the main channels at angles that falsely suggest stream flow to the w or NW. '11le pi racy has resulted from the slow westward migration of drainage divides at the heads of Middle Creek and Jennys Creek. Misfit streams provide additional evidence . The capture may be related to the late Miocene-early Pliocene regional uplift.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Rich, J. L. , 1914, Certain types of stream valleys and their meaning : Jou rnal of Geology, v. 22, p. 469-497 . Distinguishes ingrown meande r valley from intrenched meande r valle: using some examples from Arpalachians . Says that it is only when conditions lead to continuous downcutting so slow that it is equalled or exceeded by lateral cutting, yet rapid enough to �ke sweep subordinate , that the ingrown meander type of valley may be prc:xiuced.

Rich, J. L. , 1933, Physiography and structure at Cumberland Gap: Geological society of America Bulletin, v. 44, p. 1219-1236 . The lower elevation of the crest of Cumbe rland Mountain on the west side of Cumberland Gap cannot safely be used as a criterion of post-Schooley crustal movements, for it probably was produced by differential erosion alone . CUmberland Gap was not cut by a northward-flowing stream, but considerable evidence points to its having been formed by a streu& draining southward from the Middlesboro region, which has since been captured and diverted northward to CUmberland River.

Rich, J. L. , 1938, Recognition and significance of multiple erosion surfaces : Geological Society of America Bulletin, v. 49, p. 1695-1722. Questions whether multiple erosion surfaces actually exist . Critizies criteria used for recognizing such surfaces, particularly the use of ridge crests, isolated hills, and spurs as markers of former erosion levels. Too little correlation has been made between surface form and rock resistance . Uses some examples from

Appalachians•

Rich, J. L. , 1939, A bird's eye cross section of the Central Appalachian Mountains and Plateau, washington to Cincinnati: Geographical Review, v. 29, p. 561-586 . Consists mainly of photographs taken out window of passenger plane flying from Washington to Cincinnati , with extended captions for each. Flight was at low elevations , so good oblique photos were obtained .

Richards, H. C. , and Judson , S. , 1965, The Atlantic Coastal Plain and the Appalachian Highlands in the Quaternary, in Wright , H. E. , and Frey, D. G., eds. , Quaternary of the United States: Princeton, Princeton University Press, p. 129-136 . JJdson provides 1+ pages on Pleistocene frost action in the Appalachians and Coastal Plain.

Richardson, A. M., 1979, Landslide in claystone derived soil: Journal of Geotechnical Engineering Division, Proceedings of the American Society of Civil Engineering, v. 105, p. 857-869. Concludes that the shear strenth operating at the time of failure was closely related to the residual shear strength of the silt and clay-size fraction of the soil formed from the Pittsburg Redbed Claystone .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Richte r, D. M. , 1973, Periglacial feat·lref, in the central Great Smoky Mountains [Ph.D. thesis]: lthens, �. Univ1rsity of Georgia, 156 p. Attempts to infer effect of periglacial processes from examining the morphometric differences of 140 north-slope drainage basins vs . 140 south-facing basins. Looked at circularity ratio, elongation ratio, relief ratio, drainage density, and stream density. N-slope basins are more bowl shaped with ove rsteepened headwalls. In contrast, the s-slope basins show no ove rsteepened headwall, have v- shaped cross sections , and have intermittent stream channels extending to the extreme uppe r reaches of thP basins.

Riestenburg, M. M. , and Sovonick-Dunford, S., 1983, The role of woody vegetation in stabilizing slopes in the Cincinnati area, Ohio: Geological SJciety of America Bulletin, v. 94, p. 506-518. The average shear strength contributed by residual friction of the tree roots was 9 times that contributed by the residual friction of the soil. Root strength allows forested , colluvial-mantled hillslopes in the area to resist. sliding at slope angles as high as 35 degrees, whe reas similar slopes devoid of trees are subject to sliding at slope angles of 12 to 14 degrees .

Ritter, D. F., and Blakely, D. S., 1986 , Local ized catastrophic disruption of the Gasconade River flood plain during the December 1982 flood, southeast Missouri : Geology, v. 14, p. 472-476. Near Mt . Sterling, sand and gravel derived from the Gasconade channel were deposited on the flood-plain sur"-ce as a loi..;ate o. icige 30-100 m wide , 1-2 m high, and about 1 km long . A large scour hole occupying an area of 5 ha was vertically eroded ir.to the flood plain to a maximum depth of more than 7 m. Normal flood effects were exaggerated by changes made on the flood-plain surface prior to 1982 during construction of a new bridqe .

Ritter, J. R. , 1974, The effects of the Hurricane Agnes flood on channel geometry and :>ediment discharge of selected streams in the Susquehanna River basin, �ennsylvania: Journal of Research of the u.s. Geological Survey, v. 2, p. 753-761 .

·1i •.; ii1.1rricane Agnes flood seems to have hardly changed the channel geometry of the Pennsylvania streams studied in this report. The

10 sites studied generally shOio'ed that the width of the strear•. channels had been changed little by the flood and that streambed altitudes had been lowered less than a foot ( 0. 3 m) . ThF. velocity of thP streams at a given discharge had decreased.

Robinson, A. M., 1976, The effects of urbanization on stream channel morphology [M.A. thesis]: Baltimore, Johns Hopk ins University, 43 p. Studied 8 streams, ell with basins of �1t one square mi le . 3 were rural , 3 urban, 1 �rtially urbanized, and 1 undergoing development . The channel areas of the urban streams were o� the order of 2 times, and width/depth ratio 1.7 times, those of the rural streams. More cobbles and less silt and sand were found in urban ch�1els. At least 15 yr is required fo< a new equilibrium to be establ ished .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Rodgers, J. , 1948, Geology and mineral deposits of Bumpass Cove , Umcoi and Washington Counties, Tennessee : Tennessee rivision of Geology Bulletin, v. 54 , 82 p. Pages 23-24 discuss land forms . On the sides of the valley, in the outcrop belt of the �hady dolomite , are nume rous benches at various elevations. They are underlain bt residual clay, and many are capped by gravel. Reconstruction of these old valley floors by correlation of the remnants from one ridge to another is difficult and uncertain. Plate 4 shows 2 projections of the land forms , on which the benches have been emphasized. In v. rough way, these benches may be grouped into terraces which probably represent old valley floors.

Rodge rs, J., 1953, Geologic map of east Tennessee with explanatory text : Tennessee Division of Geology Bulletin, v. 58 , 168 p. Pages 11-20 describe physical geography , mainly in terms of quotations from Safford. Pages 114-121 discuss the unconsolidated mantle. Discusses residuum on different types of bedrock , footslope aprons, and isolated pebbles of quartzite far f"om major streams.

Rodgers, J. 1987 , West-runniflg brook ; the enigma of Schoharie Creek: No=theastern Geology, v. 9, p. 32-36. Schoharie Creek flows not east out of the mountains to the nearby Hudson River but we.,t and then north to the considerably more distant Mohawk River. tt.e Kaaters Kill and Platte Kill, 2 short streams draining to the kud ;on with much shorter courses and steeper gradients , have recently (Pleistocene? ) pirated a small part of the Schoharie's headwaters by cutting into the wall-like eastern front of the mountains . It is not obvious , however, why the piracy was not much earlier and much more extensive . Author suggests that before the last kilometer of two of erosion during the Te rtiary, the resistant strata, dipping westward , formed a prominent cuesta that protected the upper Schoharie from such attack .

Roehl , J. W. , 1962, Sediment source areas, delivery ratios, and influe�cing morphological factors: International Association of Scientific Hydrology Publication, v. 59, p. 202-213. Includes analysis of 15 drainage areas in S.E. Piedmont - sediment-delivery ratio as function of stream length, basin area, relief-length ratio, and weiahted mean bi furcation ratio. In some areas it appears that the reiief-length ratio is the best indicator of sediment delivery ratios, although size of drainage area will give reasonable estimates.

Rogers, H. D., 1858, Classification of the several types of orographic structure in the Appalachians and other undulated mountain-chains, in Rogers, H. D. , ed. , The Geology of Pennsylvania, Pt . 2: Philadelphia, J.B. Lippincott & Co ., p. 917-9lll. Describes the manner in which lithology and structure determines the type of topography resulting.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Rona , P. A. , 1973, Relations between rates of sediment ac�lation on continental shelves, sea-floor spreading, �� eustacy inferred from the central North Atlantic: Geological Society of America Bul letin, v. 84 , p. 2851-2872. Rates of sediment accumulation were derived from Upper Jurassic to Holocene stratigraphic columns encountered in 7 deep wells penetrating the coastal plains and continental shelf. Intervals with fast and slow rates correspond between N. America and Africa . To a fi rst approximation, the sedimentary maxima and minima are di rectly proportional to rates of sea-floor spreading in the intervening ocean basin.

Ross, R. D., 1969, Dr&inage evolution and fish distribution problems in the southern Appalachians of Virginia, in Holt, P. c. , ed ., The distributional history of the biota cf the southern Appalchians, part 1, invertebrates: Bl�cksburg, VA, VPI & State u. Research Monograph , p. 277-292. Offers a theory concerning drainage history of the New , Roanoke , and James rivers basee on fish distribution patterns and geomorphic evidence . Says the Teays ane ancestral Shenandoah once drained the region west of the Blue Ridge when both the Roanoke and James Rivers were PieJmont streaJ!!c; heading against the eastern slopes of the Blue Ridge . First the Roanoke River penetrated the Blue Ridge . After a series o1 piracies, it captured most of the present drainage of the pre�ent drainage of J3mes River west of the Ridge from the Teays River. Later the James River broke through the Blue Ridge and captured its present headwaters from the Roanoke.

Ross, R. D. , 1972, The drainage historJ of the Tennessee River, in Holt, P. c. , ed ., The distributional history of the biota of the southern Appalachians , part 3, vertebrates: Blacksburg, VA, VPI & State u. , p. 11-42. Suggests a variation of the Appalachian River theory. Latter flowed to Mobile say. The Teays was one of its tributaries. As the Appalachian River extended its headwaters, it intercepted and diverted the northwest drainages, one by one , to form the Tennessee River basin north of Chattanooga , somewhat as we now know it. Meanwhile, a tributary of the ancestral Sequatchie cut itsway through Walden Ridge and captured the Appalachian. From the biological evidence it is clear that the Tennessee River has had drainage interchanges with all its neighboring �sins.

Royster, D. L. , 1973, Highway landslide problems along the CUmberland Plateau in Tennessee : Nashville, TN, Tennessee Dept . of Transportation, 65 p. Pennington Formation is invJlved in most major landslides . Problems are worst where it is overlain by coll�:ium, which may vary from 5-10 to 40-50 ft thick over a distance of 100-200 ft. This variance is ·iue primarily to the troughs and lows filled witl. colluvium in the highly undulating and irregular sub-topography of the area. To avoid slides, one simply must be able to delineate the subsurface troughs that occur, for it is, by and large, the angle of slope along the contact between the colluvium and the shale within these troughs that determines or controls stability, rather than the cohesion and angle of friction of the individual materials.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Rozanski, G. , 1943, Stone-centered polygons: Journal of Geol09'' , v. 51 , p. 330- 341 . 0escribes and provides pictures of stone-centered polygons in New York and North Carolina.

Rubin, M. , and Alexande r, C. , 1958, u.s. Geological Sutvey radiocarbon dates IV: Science , v. 127, p. 1476-1�87 . Reports radiocarbon date of greater than 34 , 00� yr from peaty clay 13 mi N of Spartanburg, sc , and a date of gre.:.&ter than 38, COO yr from a peat laye r at Mayflower Hotel in Washin�ton, DC.

Rudisill , S. J. , 1972, The evolution of wa ter gaps in southwestern Pennsylvania [M.A. thesis ]: Pittsburg, University of �ittsburg, 66 p. Fig. 5, p. 20, shows location of all water gaps in study area. Attempts to determine origin for each : antecedent, supe rposed , or headward growth . Small streams (less than 25 mil show lack of adjustment to structure as consequence of headward growth . Large streams (greater than 35 mi) fail to correspond to structure because ot supe rposition or antecedence . Moderate size streams are of various origins. Thinks t�� e are at least 3 gene rations of streams in area.

Ruedemann , R. , 1932, I)(•·.rel;:;-�nt of drainage of Catskills: American Journal of Science , v. 23, p. 337-j�9. Concludes that ':he enUre abnormality of the Catskill drainage can be explained by systematic stream-piracy that proceeded first from the south and east and finally also from the north against the old consequent Susquehanna drainage , transforming the original symmetric southwest drainage into a more or less asymmetric north and south drainage .

Ruhe , R. v. , 1977, Summary of geohydrologic relationships in the Lost Riv� r watershed , Indiana, applied to water use and environment, in Dilamarter, R. R. , and Csallany , s. c. , eds ., Hydrologic problems in karst regions : Bowling Green, KY, �· stern Kentucky University, p. 64-78. Study topics inc �ude 1) geomorphology of the karst terrain including surficial m'terials; 2) soil, including retention capaci ty and storage capacity, permeability, transmissivity, and ability to enhance �.vff ; 3) water budget, including runoff, evapotranspi ration, subsurface flow, spring flow, subsurface storage , and hydrochemical nature of the water; 4) water use and envi ronment .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ruhe , R. v. , and Ol son , c. G. , 1980 , The origin of terra rossa in the karst of soutr.e rn Indiana , in Sha·•er, R. H., ed. , FiP.ld trips 1980 from the Indiana University Campus , Bloomington: C� ological Society of �rica North centra� Section: Bloomington , IN, Indiana Geological SuLvey, p. 84-122 . Rejects residuum as an explanation because of discrepancies between the thicknesses of terra rossa and available amounts of insoluble residue and because of the discrepancies between physical, chemical , and clay-mineral composition across sharp, abrupt terra rossa-limestone contact. Detritus from higher lying clastic rocks can be traced down and across backslopes and footslopes of erosion surfaces cut into lower lying limestone . The detr1tus is mixed with erosional debris from the lim- 5tone . The mixture weathers, but not severely, to terra roeba. The regional distribution of terra rossa is the result of the retreat of the escaq:ment .

Sackett, D. M. , and Clark , G. M. , 1985, S�rficial geol�J, geomorphology, and late Quaternary history of the Big Mountain-Butt ·�tru;;tain massif, Va lley and Ridge province , Giles County, sruthwestern Virginia [Abstract ): Geo:!.ogical Society of America Abstracts with Pmgrams , v. 17 , p. 132. On Big and Butt oountains, above 1050 m, N-fe>.cing hollows remai" damp a� are extensively mantled with slightly we�thered clasts . Sorted patterned ground occurs in the vicinity of ridge crests and is composed of sorted nets ranging up to 3 m in d:.. . .meter and sorted stripes with stone bo:�der widths of 4 .n and lengths ove r 100 !'1, Some of the saddles are perennially damp with perched water tables , offering the possibility of organic matter recovery.

Safford, J. M. , 1856 , A geological reconnaissance of the State of Tennessee : State Geologist biennial report , v. 1, p. 11-30. On p. 19-30, describes and characterizes the "natural" [physiographic) divisions of Tennessee .

Safford, J. M. , 1869, Geology of Tennessee : Nashville, TN, S.O. Me rcer, Printer to the State. Part I, Physical Geography (p. 1 -127 ) describes the physiography of the state .

Samford, w. J., 1982 , An investigation of the Narrows landslide, Giles County, Virginia [Abstract): Virginia Journal of Science, v. 33, p. 156 . The slide consists sole1y of ove rturned sandstones and shales of the Rose Hill Formation. These rocks are located on the footwall block of L�e Narrows fault �1d during ove rturning ��d thrusting were severely fractured and locally brecciated . There has been discontinuous movement of the slide since 1940 .

Sauer, C., 1927 , Geography of the Pennyroyal , Kentucky: Kentucky Geological S�rvey Series 6, v. 25, p. 5-1 30. Includes chapters on the drainage pattern and its meaning and on the physiography of various subdivisions .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Sa��d� .s, J. w. , 1985, Pine Mountaina karst and caves, in Doughe rty, P. H. , ed ., Caves and karst of Kentucky: Ken . Geol . Surv . Sp . Pub. 12, Ser. XI : Lexington , KY. !{entu -•·y Geological Survey, p. 86-96 . Descrit�� caves in Pine Mountain area . Contrasts caves in gaps and the"� on mountainsides.

Scheffel, E. R., 1920 , "Slides" in the Conemaugh Formation near Morgantown , We st Virginia: Journal of Geolo�;, v. 28, p. 340-355 . Describes slides in Conemaugh Formation.

Schlee , J. , 1957 , Upland gravels of southe rn Maryland . Geological Societ: nf America Bul letin, v. 68 , p. 1371-1401 . In the norther� part of the upland , size and composition of the gravel show orderly changes eastward, which is also the direction of sediment transport as indicated by cross-bedding ana gravel fabric. The upland deposits are fluvial in origin. They were probably deposited by a graded ancestral eastward-flowing Poton0c River.

Schmidlin, T. w. , 1986 , Does alpine permafrost exist in the northern Appalachians? , in Thi rd Conference on Appalachian Geography, Pipestem State Par�, Pipestem, wv, Mar. 14-lE , 1986 : Proceedings : Athens, wv, Concord College , p. 95-103. Based on estimates of mean aru1•li1:: air temperature , permafrost is likely ,\bove 1765 m in the Presiden�ial Range of New Hampshi re , above 900 m on the Gaspe' peninsula, ana on the uppe r 20-30 m of thP. high�st peaks of Newfoundland . Scattered patches may exist below these elevations in shaded , moist locations . Permafrost is not likely in New York or Ve rmont.

Schmidt , V. A. , 1982 , Magnetostratigraphy of sediments in Mammoth Cave , Kentucky : Science , v. 217, p. 827-829 . Clastic sediment deposits found within the cav�s of Mammoth Cave National Park have yielded a magnetostratigtaphy pattern of magnetic polarity reversals which indicate that they were deposited ove r a range of at least 1 million and most likely 2 mil 1ion years .

Schneider, R. H. , 1973, Debris slices and related flood damage resulting from Hurricane Camille, 19-20 August, and subsequent storm, 5-6 September 1969 in the Spring Creek drainage be1sin, Greenbrier County, We st Virginia [Ph.D. thesis): Knoxvi lle, TN, University of Tennessee , 131 p. A total of 1534 individual slide scar heads were found and a record made of physical characteristics. Majority of slides were concentrated in an area of approximately 58 square km, directly unde r area of most intense rainfall. Precipitation is the critical localizing agent . Slope form and inclination rank second . The most important geologic factor is lithology; rocks that weather into uniformly fine-textured soils are highly prone , whereas those that produce boulder-size blocks are not .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Schneider, W. J., 1962, Points of or1g1n of perennial rlow in Georgia · Geological Sur�ey Professional Paper., v. 450-B , p. 113-114 . Field investigations of more tr� 200 small headwater strean �alleys indicate that streamflow becomes perennial at sharply defined points, �haracterized by abrupt beginnings of incised stream heads . The chanr� · �ave semicircular heads with ve rtical walls. Depths of incisi� it the wall range from 1 to 8 ft . The valleys just upstream from the channel heads are ratl1er broad , flat flood plains covered with vegetation. Streams that are epheme ral throughout their length to their junction with a perennial stream have ger,erally convex profiles, vs . concave for initially perennial streams .

Schu.ltz , A. P. , 1986 , Ancient , giant rockslides, Sinking Creek Mountain, southern Appalachians : Geology, v. 14, p. 11-14 . Individual blocks are as long as 5 km. The zone of rockslides, identified by anomalous topography and geologic structures, is about 25 km long and 1 km wide . Downslope transport, from 0.5 to 1 km, of at least 100 million cubic meters of Silurian sandstones and shales can be identifield. During Eliding, bedding within individual blocks has unde rgone 30 tu 90 degree rotation about a horizontal axis. The displaced masses have undergone extensive erosio11 and dissection . Zone is located within 15 km of Giles County seismic zone .

Schultz, A. P., 198'/ , Failure kinematics of ancient giant rC":..:k block slides and rock slumps, southern Appalach: .n Valley and Ridge province [Extended abstr3ct): u.s. Geological Survey Circular, v. 1008 , p. 32-33. Tht kinematics of the failures can be inferred from �� variety of rockslides present . Fig. 10.1 illustrates various stages of failure of giant rock block slides and slumps. Where dips of beds are relatively high (45 degrees or more), relatively small slump blocks form with downslope displacement. �ere dips are less than 30 degrees, relatively large rock block slides form that move downslope as coherent sheets.

Schultz , A. P., 1987 , Sinking Creek Mountain, Virginia, rock block slide complex: Excerpt from the Southeastern Section Geological Society of America field trip road log: u.s. Geological Survey Circular, v. 1008 , p. 40-42 . The topographic, structural , and stratigraphic data suggest that large sections (100 to 500 mill ion cubic meters) of the southeast flank of Sinking Creek Mtn ��tached along bedding planes and joints and slid downslope . Initial detachment was probably near the Rose Hill-Keefer contact and/or in the upper part of the Rose Hill Formation. During the early stages of sliding, the blocks unde rwent translational sliding parallel to bedding on the upper dip slopes . Continued movement lowe r or. the mountain included rotational sliding. After emplace�nt , large parts of the slide failed �1 slumping. A maximum age of 2 m.y. i� suggested for rockslide emplacement .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Schultz , A. P., and Southworth, C. S., 1987, Landslides of eastern North America: U.S. Geological Survey Circular, v. 1008, 43 p. Contains extended 17 abstracts relating to landslides in the eastern u.s., many of which deal with locations in the Appalachians .

Schultz, D. , and Pumroy, C. , 1980, Fourier shape ru> alysis o( dolines in the Mamooth Cave plateau regic.1 of Kentucky [Abstract I : Geological Society of America Abstracts with Prcgrams, v. 12, p. s· �. Data indicate that dol1ne populations from each formation can be distinguished from one another by visual inspection of the mean harmonic amplitude spectra and by statistical analysis of the shape frequen� distributions, especially in the higher harmonic components which represent detailed shape variations .

Schumm, S. A. , Mosley, M. P., Zimpfer, G. L. , and Trimble, S. w. , 1976, Unsteady state denudation: Science, v. 191 , p. 871. Schumm, Mosley, and Zimpfer respond to Trimble's 1975 Science article, and Trimble replies . Schumm et al say the question "Can we assume steady state?" can always be answered negatively, over the span of time involved , regardless of man's effects . Trimble responds that his main point was that denudation rates based merely on sediment yield may have little meaning unless sediment storage (colluvium and alluvim) is considered .

Schwarcz , H. P., Harmon, R. S. , Thompson , P. , and Ford, D. C., 1976, Stable isotope studies of fluid inclusions in speleothems and their paleoclimatic significance : Geochimica et Cosmochimica Acta , v. 40, p. 657-665. Fluid inclusions found trapped in speleothems are interpreted as samples of seepage water from which enclosing calcium carbonate was de�sited . '!he inclusions are assumed to have preserved their D;1i ratios since time of deposition. Estimates of temperatures of deposition of the carbonate can be calculated from inclusion D/H ratios and delta-18 of oxygen. Includes speleothems from Man'IIIOth cave , KY, and Greenbrier County, WV.

Schwarz, F. K., 1970, The unpr�cedented rains in Virginia associated with the remnants of Hurricane Camille: Monthly Weather Review, v. 98 , p. 851-859 . Concludes that the extreme rains, concentrating a little to the north of the track of the remnant� of camille through Virginia, were within about 80-85 percent of probable �imum values for areas up to 1,000 squa re miles for a duration of 12 hr.

Scott, R. C., 1981, Weather conditions associated with major debris avalanche occurrences in the southe rn Appalachians , in Hill , P. T. , ed. , Conference of Appalachian Geography , Pipestem State Park , Pipestem, wv, Oct. 2-3, 1981: Proceedings : Athens , wv, Concord College , p. 26-36. States that the Great Smoky Mountain area has the most debris avalanches in the ��lachians , and attributes this to several factors. First, the area receives by far the heaviest rainfalls in the Appalachians, due to the elevation of the peaks (highest in the Appalachians ) and southerly location (in an optimum location to intercept moisture-bearing southwesterl y winds from the Gul � of Mexico). warmer temperatures and abunoant rainfall also enhance chemical weathering that produces regolith.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Scott, R. C. , Jr. , 1972, �he gP.omorphic significance of debris avalanching in the Appalachian Blue Ridgo Mountains [Ph.D. thesis] : Athens , Georgia, University of Georgia, 185 p. Suggests that creep and debris avalanching play complementary roles in transporting regolith which forms on steep slopes to surface streams . Creep moves debris into hollows , and debris avalanches periodically flush it out. Notes that debris avalanches seem to become progressively less common going west from the Blue Ridge through the Valley and Ridge to the Appalachian Plateau, probably because rocks become weaker. Describes post-slide recovery processes .

Scully, w. S., and Arnold, R. w. , 1978, Holocene alluvial stratigraphy in the uppe r Susquehanna River basin, New Yo rk : Quaternary Research, v. 15, p. 327-344 . Two alluvial terraces and the present flood plain were studied at two locations along the Susquehanna and unadilla Rivers in south-central New Yor� .

Segovia, A. v. , 1974 , Geology and geochronology of the Shenandoah Valley in the Flint Run area, in Gardner, w. M. , ed ., The Flint Run paleo-indian complex : Washington, DC, Catholic University of America, p. 48-65. Describes physiography, alluvial stratigraphy , geochronology (one radiocarbon date ) of paleo-indian site.

Segovia, A. V. , 1981, Archeclogical geology of the Savannah River valley and main tributaries in the Richard B. Russell Multiple Resource area: Atlanta , GA., Archeol . Serv. , Nat . Park Service , 93 p. Developed a conceptual IOOdel for the evolt''":.on of morphologic elements in the area, in both the floodplain and the islands, which could be used in relative dating and correlation of the major stratigraphic units and depositional discontinuities . A recustruction of the landscape at various stages in the evolution of the valley, from the Pleistocene to the present , is presented . We ll illustrated with sketches.

Segovia, A. v. , and Franco, L. , 1977, Archaeological implications of the geomorphologic evolution of the lower Shenandoah Valley, Virginia: New York Academy of Scie�ces Annals, v. 288, p. 189-193. The levels of terraces above the present floodplain are 60, 130, 230, 330, and 450 ft. A rough approximation of the average rate of downcutting of the stream was previously estimated by Segovia at 1 m per 10,000 yr , in which case the ages of these terraces would range from 200,000 to 1,500, 000 yr . (These ages would be roughly doubled by using Hack 's estimate of 40 mmVl,OOO yr .) Continuous lateral migration of the South Fork results in a pattern of deposition in which isochronous surfaces are not hor zontal within the body of the alluvium but separate a succession of slices that are younger both laterally towards the stream and upwards .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Seven , W. D. , 1967 , The Bowmanstown boulder ��2ld , Carbon County, Pennsylvania : Pennsylvania Academy of Science Proceedings , v. 40, p. 90-94 . A 0.75-mi long field of subrounded matrix-enclosed Palmerton sandstone boulders averaging 1 to 2 ft in diameter occurs in the axial valley of an overturned anticline . The field surface has a gradient of 5 degrees and :;.s covered with vegetation except whe re the matrix has been removed by headward erosion . Field evidence indicates that the boulders were transported to their present locations from outcrops immediately to the north by rock-glacier creep. (The low matrix content suggests that the internal friction would probably have been too high to allow movement by solifluction, so that freezing and thawing of interstial water has to be appealed to .)

Seven , w. D. , 1969, Sedimentology of some Mississippian and Pleistocene deposits of northeaster .. Pennsylvania, in Subitsky, S., ed. , Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions : New Brunswick, NJ, Rutgers University Press, p. 214-234. On p. 221-227 , describes boulder fields in Carbon County, concentrating on Hickory Run boulder field. Fig. 10 is a very large-scale map of the field, showing mounds, depressions, and stone rings; shows complex microrelief. At Hickory Run, gene rQlly cobbles and smaller boulders are confined to high centers of microrelief features and larger boulders occupy lower parts of microrelief features . Boulders decrease in size and increase in roundness both with depth and down field. Suggests that during formation of the field, the amount of fine-grained material was minimized and that during deglaciation the fines moved down and formed the matrix. Notes many forested boulder fields do not possess interstitial matrix, but rathe r the uppe r surfaces comprises a 1-2 ft thick humic layer which is unde rlain by empty interstices.

Sevon , w. D. , 1972, Late Wisconsinan periglacial boulder deposits in northeastern Pennsylvania [Abstract]: Geological Society of America Abstracts with Programs , v. 4, p. 43-44. Two types of boulder deposits occur on latest Wisconsin till. The first is boulder colluvium, which occurs on low to moJerately steep slopes as surficial boulder accumulations 1-2 boulders thick overlying either undi sturbed or cryoturbated till . Boulder density ranges from local concentratj ons forming stone stripes to complete surface cove rage . The seLond is boulder fields, consisting of flat-surfaced, valley-bettom boulder concentrations several feet thick . The boulder fields lack size sorting, matrix, rounding of boulders, or detectable flow-developed structures. Both deposits occur in a zone 1-2 miles wide south of an end moraine located several miles north of the Wisconsin "terminal moraine ." The deposits become progressively less well developed , both in form and areal extent , southward from the end moraine margin.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Sevon, W. D. , 1975, Sandstone saprolite, roundst�ne diamicton and the Harrisburg peneplain in eastern Pennsylvania [Abstract ): Geological Society of America Abstracts with Programs , v. 7, p. 118 . The saprolite underlies the crest of a flat-topped interfluve whose uppe r surface is considered to be part of the Harrisburg peneplain. It is interpreted as the product of chemical weathering under conditions of minimal erosion in a more humid and temperate climate. It may be the first evidence , other- than accordant elevations, to support the reality of a Harrisburg peneplain.

Sevon, W. D. , 1985, Pennsylvania's polygenetic landscape : Guidebook for the 4th Annual Field Trip of the Harrisburg Area Geological Society: Harrisburg, PA , Harrisburg Area Geol . Society, 55 p. Addresses problems involving drainage evolutiJn of the Valley and Ridge in Pennsylvania: Initial position of the dr,:�inage divide and the direction of drainage , time and origin of sout'1east drainage , peneplains, question of Cretaceous transgression, timing of uplift, transverse drainage , rate of denudation, and landscape age . Proposes a model for the development of Pennsylvania's landscape . Offers evidence for the existence and age of the Harrisburg peneplain. An excellent review and discussion.

Sevon, W. D., Potter, N., Jr., and Crowl , G. H. , 1983, Appalachian peneplains: An historical ove rview: Earth Sciences History, v. 2, p. 156-lu4. Reviews ages and correlations which have been suggested for erosion surfaces in the Appa lachians. Also discusses the history of research on peneplains, geological phenomena that have been suggested to be dependent upon peneplanation, attacks on the peneplain concept, and current status of the peneplain �oncept .

Shafer, D. s. , 1984, Late-Quaternary paleoecologic, geomorphic , and paleoclimatic history of Flat Laurel Gap, Blue Ridge Mountains, North Carolina [M.S. thesis): Knoxville, TN, University of Tennessee, 148 p. Analysis of colluvial and fluvial deposits, fossil pollen spectra , and plant macrofossils provide a late-Quaternary record of landscape evolution. Thermoluminescence analysis provides the absolute-age determinations for periglacial 1eposits in the Southern Appalachians . The Pleistocene/Holocene transition, dated by TL between 11,900 and 10, 100 yr , represents a period of climatic amelioration and a changeover from colluvial to alluvi al processes . A TL date of 7400 plus or minus 1000 yr for sediments within a blockstream entering the bog indicates that Pleistocene periglacial material may have been reworked during a wet episode of the Holocene .

Shaffer, P. R. , 1945, Erosion surfaces c,f the �>outhern Appalachians [Ph.D. thesis): Columbus , OH, Ohio State University, 99 p. One peneplain, two erosion surfaces, and a surface or strath are present in the southern Appalachians , if the present or recent valley floors are excluded. These surfaces are, from oldest to youngest: 1) Upland peneplain, 2) �umbe rland erosion surface , 3) Va lley erc �ion surface , and 4) Coosa strath. cut-out projected profiles of the Barrell type were prepared for the area of detailed study . Surfaces were correlated with well-recognized erosion surfaces of the northern Appalachians .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Shaffer, P. R. , 1947, Correlation of erosion surfaces of the southern Appalachians : Joumal of Geology, v. SS, p. 343-352 . Zonal profiles and field observations indicate that one peneplain , two erosion surfaces , and a minor surface or strath are present in the southern Appalachians, not considering present or recent valley floors. These surfaces are correlated with the well-recognized erosion surfaces of the northern Appalachians . The effect cf structure upon the de 1elopment of the erosion surfaces is considered.

Shaler, N. s. , 1899, Spacing of rivers with reference to hypothesis of baseleveling: Geological Society of America Bulletin, v. 10, p. 263-276 . Argues that the reason for approximate equality of summit altitudes throughout an area is not because of a former erosion surface , but because streams tend to be approximately equally spaced.

Sharp, C. F. S., and Dosch , E. F., 1942 , Re lation of soil-creep to ear �flow in the Appalachian Plateaus: Journal of Geomorphology, v. 5, p. 312-324. Road cuts arn auger borings reveal that beds of coal , clay, and shale, instead of extending horizontally to i��grsect the hill surface, thin abruptly and bend down slope, approaching the ground surface only gradually. Creep of coal and clay at the outcrop was clearly described in 1856 by Lesley. Where clay or ��ale layers are drawn out subparallel to the hill slope, these impervious layers interfere with the downward percolation of surface water. Earthflows are IIX.lst likely to occur above sags or troughs in the impervious layer .

Sharp, H. � .• 1929, The Fall Zone peneplain: Science , v. 69 , p. 544-545. Proposes that the Coastal Plain basement and its uncovered extension is a distinct peneplain and not as formerly supposed the continuation of the upland surfaces . Notes that this peneplain stretches from ronnect.icut to Georgia in a long narrow belt or :.-one seldom 15 miles wide between the more gently sloping upland peneplain and the coastal Plain. It ave rages perhaps 50 ft;mi in slope .

Sharp, H. s., 1932, The geomorphic developmen� of central Ohio: Denison University Bulletin, Journal of the Sci . Lab. , v. 27, p. 1-46. Presents landscape development in terms of erosion cycleG followed by glacial modification.

Sharp, H. s., 1933, The origin of Mountain Lake , Virginia: Journal of Geology, v. 41, p. 636-641 . Author says that all the features he notes indicate origin of the lake basin as a normal stream subsequently damrred by talus .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Sharp, H. s. , 1S45, Stream selectivity in the middle Appalachian Va lley: Journal of Geologj, v. 53, p. 200-205. By differential erosion the limestone areas have been lowered considerably below the level of the shales, but , in spite of this obvious weakness of the limestones, Conococheague Creek and other streams show remarkable adjustment to shale belts. These courses are interpreted as subsequent and as due to the greater �akness of the shales toward concentrated stream erosion, whereas the limestones have been dissolved by unconcentrated rainwa sh.

Shaw, E. W. , 1911, High terraces and abandoned valJ �ys in western Pennsylvania : Journal of Geology, v. 19, p. 140-156. Development of high terraces and abandoned parts of valleys of western Pennsylvania seems to have been caused by the development of a valley train over 100 feet thick along the Allegheny and Oh io. In the tributaries of these streams , aggradation began at the mouth and extended upstream. Eventually these rivers found themselves flowing at the height of one after another of the lowest places in nearby divides, and at such times and places flow through cols occurred. When the final dissection began, the rivers chose the channels momentarily most desirable , and in many cas�s were superimposed on hard rock where nearby were courses through unconsolidated wa terial .

Shaw, E. w. , 1918, Ages of peneplains of the Appalachian Province : Geological Society of America Bulletin, v. 29, p. 575-586. Data which are generally available indicate that all peneplains of which remnants exist today are younger than the floor under the Cretaceous with which one or more have so frequently been correlated. Opines that no portion of any surface so old as early or even late Mesozoic can have endured until the present day .

Sheehan , M. c. , Whitehead, D. R. , and Jackson, s. T., 1985, Late Quaternary history of the Richard B. Russell Multiple Resource Area , in Russell Papers 1985, Interagency Archeological Services, National Park Service : Atlanta, GA, National Park Service, 37 p. Palynological data from three sites allowed the reconstruction

of a vegetational sequence from 22, 000 yr B .• . to the present. Five vegetational periods were delineated: Full Glacial, Late Glacial, Early Postglacial, Mid-postglacial , and Late Postglacial .

Shepps , v. c. , 1962, P�nnsylvania and the ice age : Pennsylvania Topographic and Geologic Survey, Educational Series, v. 6, 30 p. A popular account of the Quaternary history of Pennsylvania.

Simmons , G. c. , 1966, Stream anticlines in central Kentucky: U.S. Geologi :al Survey Professional Paper, v. 550-D, p. D9-Dll. Small nontectonic foldc called stream anticlines occur in �nterbedded limestone and shale of the Upper Ordovician in central Kentucky. Although their amplitude commonly is only a few feet, some anticlines are more than hal f a nule long ; most are fractured along their crest. Stream anticlines c_e unrelated to tectonic features, and their coincidence with \ _ley bottoms suggests a Recent origin. This origin is substantiated at one place by an eyewitness account.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Simonson , R. w. , 1982, LOess in soils of Delaware, Maryland , and northeastern Vi rginia: Soil Science , v. 133, p. 167-178. Thick silt mantles (> 100 em) provide materials for at least the entire solum and occur only in the Coastal Plain near the margins of Chesapeake Bay and Delaware . Intermediate mantles (40-100 em) provide materials and the A and E and for much but not all of the B horizon. Intermediate mantles are more widespread in the Coastal Plain than in the Piedmont . Thin silty nantles (usually < 30 em) provide materials for A and E horizons or become silty components of upper horizons . These mantles are widespread in the Piedmont . Five lines of evidence are presented to support the interpretation of silty mantles as loess.

tiimpson , c. T. , 1900, On the evidence of �, e Unionidae regarding the former courses of the Tennessee and other Southern rivers: Sciences, N.S., v. 12 , p. 133-136 . The similarity of Unionidae in the Tennessee and Alabama drainage systems suggests that sometime in the middle or later Tertiary, the Tennessee River must have flowed southward into some one of the streams of the Alabama drainage , and through this to the Gulf of MP.xico.

Simpson , P. s. , and Simpson, J. H. , Jr ., 1970, Torn land : Lynchburg, VA, J.P. Bell Co ., 429 p. A non-geologic account of the floods and debris avalanches, centereci on Nelson County, that accompanied the 1969 Hurricane Camill� storms . There are some good eye-wi tness accounts, such as that o·.1 p. 343-344 , furnishoo by two moonshiners who were JP in a hollow when the ground began to move .

Sinnott, A. , and Cushing, E. M. , 1978, Summary appraisals of the nation's ground-water resources - Mid-Atlantic region: U.S. Geological Survey Professional Paper, v. 813-I , p. Il-!32 . Gives brief accounts of relation of occurrence of qroun- dwater to the bedrock and surficial geology of each physiographic province .

Siple, G. E. , 1964, Geohydrology of storage of radioactive waste in crystalline rocks at the AEC Savannah River Plant , S.C. : u.s. Geological Survey Professional Paper, v. 501-C, p. C180-Cl84 . Geologic, hydrologic, and water-quality studies indicate two distinct aquifer syst'!.'ms at the savannah River Plant : one in crystalline basement rock, and the other in the overlying 900-ft sequence of sedimentary strata . A confining layer of saprolite separates the two systems , preventing significant exchange of water between them and retarding circulation within the crystalline rocks. The saprolite formed in a subaerial environment when the basement rocks were exposed to weathering p:ior to the deposition of the Tuscaloosa matioFor n in Late Cretaceou£ time .

Siple, G. E. , 1967, Geology and ground water of the Savannah River plant and vicinity, Stmth Carolina : U.S. Geological Survey Wate r-supply Paper, v. 1841, 113 p. A detailed account that is essentially summarized by Siple 's 1964 article.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Sirkin, L. A. , Denny, C. S. , and Rubin, M. , 1977 , Late Pleistocene envi ronment of the central Delmarva Peninsula , Delaware-Maryland : Geological Society of America Bulletir., v. 88 , p. 139-142. Th� Parsousburg Sand , which is part fJ.uviatile and f:lrt eolian, mantles terraces and uplands in the central Delmarva Peninsula . Its organic horizons are fresh-water peats, which range in age from about 30,000 to 13,000 yr . Pollen assemblages in the sediments suggest colder and perhaps drier conditions than at present .

Sites , R. s. , 1973, Geology of the Smoke Hole region of We st Virginia: Southeastern Geology, v. 15, p. 153-167 . Discusses the manne r in which bedrock 3t ructure has affected physiography , drainage pattern, and drainage evolution in the area.

Smart, J. S. , and Moruzzi , V. L., 1971 , Computer simulation of Clinch Mountain drainage networks: Journal of Geology, v. 79, p. 572-564. Clinch Mountain provides an excellent example of a system with uniform lithology and structure but varying structural parameter�. Va rious properties of the stream networks were measured and analyzed as a function of dip angle . A random-walk headward-growth model of stream network development was used to simulate the Clinch Mountain network .

Smith, H. T. U. , 1949, Physical effects of Pleistocene climatic changes in nonglaciated areas : Eol ian phenomenoa , frost action, and stream terracing: Geological Society of America Bulletin, v. 60, p. 1485-1515. Includes Appalachians in his discussion of the following possible relict periglacial features: ground-ice wedges, solifluction deposits, blockfie1ds , involutions , stone rings and stripes, earth mounds or palsen, amorphous disturbed soil, landslides, stabilized taluses, nivation hollows , protalus ramparts, minor superficial folds , dry valleys , asymmetric valleys , and stream terraces.

Smith, H. T. u. , 1953, The Hickory Run boulder field: American Journal of Science , v. 2Si , p. 625-642. The field lies within an area mapped as Illinoian drift, just beyond the border of the Wiscor.�in drift. Surface gradient is close to 1 degree . The lllC'Iphology and lithology of the boulder field, together with i�s present aspect of stagnation and decay , are best explained as resulting from periglacial climatic conditions during the near approach of the Wisconsin ice sheet . it is the largest boulder field in the Appalachian region . The barreness is probably a secondary feature , due to the gradual flushing of interstitial fines by runn ing water. Gra��al extension of flushing upvalley would account for the somewhat more weathered appearance of boulders at the lower end .

Smi th, H. T. u. , 1962 , Pe riglacial frost fedtures and related phenomena in the united States: Biuletyn Peryglacjalny, v. 11, p. 325-342. Discusse!> nume rous possible relict periglacial features in the unglaciated Appalachians , among oth&r places .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Smith , H. T. u. , 1968, Piping in relatio� to periglacial boulder concentrations : Biuletyn Peryglacjalny, v. 17, p. 195-204 . Earlier Smith proposed that boulder fields represent modification of a periglacial �le sheet with a matrix of fines. He notes the problem of removing fines by nlnL"ling water - that of how to remove them from beneath the boulders - and proposes piping as a mechanism. This would also help to explain depressions in the boulder fields.

Smith, L. L. , 1941, Weather pits in granite of the southern Piedmont : Journal of Geomorphology, v. 4, p. 117-127. The largest pits are about 40 ft in diameter and 2-3 ft deep . Suggests that the pits are initiated by small slight concavities produced by spalling. After a miniature pit is started , weathering in tr�t place is accelerated by the greater action of moisture and acids formed by the decay of vegetation.

Smyre , J., 1977, Some thoughts on the analysis of dissolution scallops , based on observations in Dance veCa , Big Bone Cave , and cumberland Cave rns , Tennessee: Speleonews , v. 21 , p. 53-66 . The rather low paleoflow velocities in Big Bone and in cumberland are adequate to transport, particularly in suspension, the red claye , silts, and fine sands that are douti.nant. fill materials in bot_!- , caves . Also discusses limitations of scallop analysis.

Sonderegger, J. L., 1974, Effect of Chattanooga Shale facies distribution on the in situ formation of negative structures by ground-��ter solution [Abstract] : Geological Society of America Abstracts with Programs, v. 6, p. 399. Basins and synclines observed in Devonian and Mississippian age formations along the Highland Rim of Alabama are presently forming by solution of the underlying Ordovician limestones. This preferential solution is controlled by physical and chemical variations within the Chattanooga Shale, which acts as a regional aquitard. A bituminous member accounts tor most of the increase in thickness i11 thicker sections, and is rich in pyrite, which controls ground water acidity. Thus , incre3sed solution of limestones occurs heneath the thickest sections of the Chattanooga Shale.

Sapper, w. E. , 1971, Characteristics of streamflow of small watersheds in Pennsylvania and factors that influence :. t: Pennsylvani<� State university Inst. for Research on Land and Water Re�;ources, research project technical completion report A-006-PA: un.�versity Park , PA , Pennsylvania State university, 14 p. Attempted to relate various flow indices to watershed parameters, the latter including physiographic region, latitude , and forest cover.

Sapper, w. E., and Lull, H. w. , 1965, Streamflow characteristics of physiographic units in the Northeast: Water Resources Research, v. 1, p. ll5-124. Although there were significant differences between catchments within each division, the divisions each possessed distinctive characteristics of stream flow.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Southworth , c. S., 1987 , Prehistoric giant rockslides of the Appalachian Va lley and Ridge province : Types and characte �istics [Extended abstract ): U.S. Geological Survey Circular, v. 1008 , p. 24-32 . Four different types of prehistork giant rockslides have been recognized: rock slumps , rock block glides, rock avalanches, and debris avalanches, all dip-slope failure:; on anticlinal fold limbs . The rockslides involve predomin��tly sandstone and quartzite, with the detachment plane located near a basal shale and/or limestone contact. Individual rockslides have d_.�nsions as large as 2.5 km by 4.3 km. Volumes range from 3 million to 1 billion cubic meters. Fig. 9.1 shows locations , Table 9.1 shows characteristics of the 4 main types, Table 9.2 shows characteristics of specific slides , Ftg. 9.2 shows aerial photos of 4 slides, Fig. 9.3 shows maps of same 4 slides . The gia�t rockslides are relict features cf extreme erosive, climatic, andjor seismic conditions never before realized ir. this area. The different aJOC>Unts of subsequent erosion suggest that the rockslide process has been active for a long ti� .

Sowers, G. F. , 1954, Soil proble� in the southern Piedmont region: American Society of Civil Engineers Proceedings , Separate 416, v. 80, p. 416 .1- 416 .18. Discus�es mechanical properties of and engineering problems associated witb s0ils of the Piedmont .

Sowers, G. F. , 1963, Er.gineering properties of residual soils derived from igneous and metamurphic rocks, in Second fanamerican Conference on Soil Mechanics and Foundations Engineering, p. 39-62 . Discusses mechanical problems of soils derived from crystalline rocks, using examples from the southeastern u.�. among others .

Spangler, L. E. , 1982, Karst hydrogeology of northern Fayette and southern Scott Counties, Kentucky [M.S. thesis) : Lexington, KY, University of Kentucky, 103 p. Dye tracing used to outline groundwater basins of springs . Groundwater flow within these basins has a dendritic pattern, with nume rous inputs resurging at one output . Groundwater flow and solution development are greatest in the central and downstream parts of the basin; along groundwater divides , solution development is less apparent and surface drainage is more extensi'!e . Groundwater divides generally do not correlate with surface divides in the larger basins, but do in the smaller ones .

Spangler, L. E., and Thrailkill, J., 1981, Hydrogeology of northern Fayette County, Kentucky, in Beck, B. F. , ed., Eighth International Congress of Spel oology: Huntsville, AL, NSS , p. 553-555. Flow patterns appear to be dendritic and the development of both surface karst features and the size of conduits appears to be related to position in the basin, being greatest in the central and downstream portions and least near divides, which may or may not underlie surface divides. The major conduits in the Royal Springs and Slack Spring basins are apparently related to master joints or unmapped faults which trend down the regional dip, but the controls of solutional development elsewhere are less obvious .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Springer, M. E. , and Elder, J. A. , 1980 , Soils of Tennessee : Un iversity of Tennessee Agricultur�- Experiment Station Bulletir., v. 596 , 65 p. Has map showing major soils in Tennessee , also has fairly detailed discussions of soils in each physiographic region .

Staheli , �. C., 1974, Stone Mountain, Georgia : Monadnock or sea stack? [Abstract]: Geological Society of America Abstracts with Programs, v. 6, p. 965 . Suggests that, as Stone Mountain lies on the part of the Piedmont that may have been subject to marine transgression, it may possibly be a sea stack . The relatively large area of exposed granite south and cast of the mountain can be explained by marine terracing.

Staheli, A. c. , 1976, Topographic expression of supe rimposed drainage on the Georgia Piedmont : Geological Society of America Bulletin, v. 87 , p. 450- 452. The Brevard zone separates two regions on the Georgia Piedmont that have different drainage stylP.s. Streams on the NW Piedmont have trellis drainage , which suggests t� t they have unde rgone a different evolution than streams tha t have dendritic drainage , on the southeastern Piedmont . It is concluded that Coastal Plain sediment covered the southeastern Georgia Piedmont to at least the Brevard zone . Consequent streams developed a dendritic drainage on this cover and became superimposed across buried resistant northeast-trending geologic structures. Trellis drainages, however, developed as a result of subsequent streams being controlled by Piedmont structures on areas of thin or no Coastal Plain sediment cover.

Staheli- �- C •• 1977 , Geologic significance of riverine swamp distribution on the Geor':>e' Piedmont [Abstract ]: Geological Society of America Abstracts witi: P;r� ams, v. 9, p. 186. MI.:: c than 1000 s,.ramps were classified into 1' structure controlled; 2) mdn-induced; 3) gradient-influenced swamps caused by a decrease in streum gra1ient �ther than 1 and 2, such as locations behind natural levees, in oxbows , or at the junction of tributaries onto the floodplains oZ l�rg�• �treams. 90 percent of all Piedmont swamps occur SE r.. c t.;e Brev.ud zone in drainage basins of streams that flow normal w r�;iion:.l structurP.s . The Pine Mountain nickpoint is the most influential control ove r the lccation of swamps on �� e Georgia Piedmont .

Staheli , A. C., Ogren, D. E., and Wharton, c. H. , 1974, Age of swamps in the Alcovy River drainage basin: Southeastern Geology, v. 16, p. 103-106. BasicalJy this is an atlack on Trimble's 1970 p3per which claimed Lhat th� Alcovy River swamps are post-settlement in age . Six samples of organic materi�ls taken at depths of 1.6 to 13.3 ft bel�g the swamps on the flood plains that comprise the drainage basi.n have radiocarbon dates that range from 1785 A.D. to 6750 B.C. Duropean colonization and agricultural activity on the Georgia Piedmont !::egan about 1814 . It is thus concluded that the Alcovy Ri ver swamps were caused by natural processes .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Staheli , A. c. , Ogren, D. E., and Wha rton, c. H. , 1977, The age of the Alcovy swamps : A reply: Southeastern Geology, v. 18, p. 195-198 . A reply to Trimble who attacked their 1974 p�per which attempted to prove the antiquity of the Alcovy swamps , as oppos,1 to �ing the products of post-settlement erosi�n and sedimentation. They reaffirm their cla1m, and note that low rates of sedimentation in the swamps do not necessarily conflict with high rates of �rosion on the uplands .

Stanley, s. R. , and Ci.olkosz, E. J. , 1�81, Classification and genesis of spodosols in the central Appalachians: Soi.l Science Society of America Journal , v. 45, p. 912-917. Al, Fe , and C appear to accumulate in spodic hor1zons of well-drained soils in colder areas of the Appalachians to a greater extent than in warmer areas and result in a more strongly expressed Spodosol in the cooler areas.

Stearns , R. G. , 1967 , Wa rping of the We stern Highland Rim peneplain in Tennessee by ground-water sapping: Geological Society of America Bul letin, v. 78, p. 1111-1124 . In this area, there is close similarity in the configuration of the upland , the structure of the base of the Cretaceous , and the erosional levels of graded streams. sus ..,, ;ts that the stream-flow system extends its erusional influence beneath the rim, and the inward-sloping surface of the old cpland (capped by Cretnceous outliers) sags toward the inc1sed streams because of ground-water sappi11g.

Stearns , R. G. , and Reesman, A. L., 1986 , Cambrian t· ·, ":--'oc...,ne structural and burial history of Nashville Dome : MPG Bulletin, v. 70 , p. 143- 154. At least 2, 290 m of post-Devonian strata have been removed by erosion . Mesozoic to Holocene uplift was at least 1,940 m, 460 m (25 %) �[ which occurred in the latest 100 m.y. and 140 m (7 %) during the latest 2 m.y. , a rate ranging from about 4.6 rovm .y. for the longer term to over 70 m;m.y. in the Pleistocene to Holocene .

Stearns , R. G. , and Wilson, J. M. , 1971, Hydrology, geology, and erosion by leaching in Skillman basin on the Western Highland Rim, Lawrence County , Tennessze : Tennessee Division Water Resources Wa ter Resources Research Series, v. 3, 33 p. The basi.n, 2.57 square miles in area, is underlain by thin soil and colluviur· bennth which j s bed..;ed wti jointed cher:t saprolith which exter.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Stephens, E. P. , 1956 , The uprooting of trees, a forest process : Soil Science Society of America Proceedings , v. 20, p. 113-116. Uprooting was establisherl conclusively as an important factor in the development of the area during the last 500 yr . Fig. 1 - Contour map of forest floor with 6-inch contour interval. Figure 2

- Map of mound and pit surfaces, 1450-1952 A.D. Fig. 3 - Gross anatomy of mounds and pits, showing 4 major anatomi cal features . Almost 14 % of the surface of the present forest floor is composed of mounds and ri ts.

Stephenson, S. L. , 1982 , A gradient analysis of slope forest communities of the Salt Pond Mountain area in souti-:westem Virginia: Castanea , v. 47 , p. 201- 215. Factors related to environmental moisture seem to have the greatest influence on the vegetation, whe reas factors related to ele•Jation and differences in soil parent materials are of secondary importance in accounting for the observed pitterns of vegetation.

Stockdale , P. B. , 1936, Montlake - an amazing sinkhole : Journal of Geology, v. 44 , p. 515-522 . Montlake , located on the CUmberland Plate�u near Chattanooga , is wa!led with massive sandstone . In spite of its situation 800 ft above limestone beds , it is thought to have originated by collapse of hund reds of feet of strata into a large cavern.

Stose , A. J., and Stose, G. W. , 1946, The physical features of Carroll County and Frederick County: Baltimore, MD, Maryland Board of Natural Res. , 131 p. Geography ana physiography sections are useful .

Stose , G. w. , 1904, Phy.;.wgraphic studies in southern Pennsylvania: Journal of Geology, v. 12, p. 413-484. Describes phys iography and relation to bedrock . Also discusses peneplains .

Stose , G. w. , 1927 , Possible post-cretaceou� faulting in the Appalachians : Geological Society of America Bulletl.1, v. 38 , fl· 493-504 . Correlation of peneplains in Vf.,J.ley and Ridge , Blue Ridge , ar� Pitdmont is suggested in table . From these correlations he inferred offsets and thus Cenozoic faulting.

Str.,;e , G. W. , 1928 , High gravels of Susquehanna River above Columbia, Pennsylvania: Geological Society of America T3ulletin, v. 39, p. 1073·-1086 . The highest gravels were found on benches in th� Hellam Hills, southwest of Matietta, PA , 500 ft above the river. Discusses lower gravels, their correlations, and relation to glaciations . Hlgher gravels are correlated and related to peneplains. Correlates the high-level gravels with the Brandywine Formation at the mouth of the river. Suggests that the high gravels are much older than the Bryn Ma� r gr3vels, which strew the upland surface on the margin of the Coa�tal Plain, and that they are of e�rly Tertiary or possibly late Cretaceous age .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Stose , G. w. , 1930, Is the Bryn Mawr peneplain a warped surface? : American Journal of Science , v. 19, p. 178-184. Takes issue with Campbell 's 1929 paper in which he suggestPd that the Bryn Mawr gravels indi cated deformation of the Piedmont surface . Thinks Campbell has erred in correlating gravels, and he presents projected profiles to prove his point. Says that a simple upl ift with tilting towa rd the sea may be assumed for the Bryn Mawr plain, rather than the anticlinal warping proposed by Campbell .

Stose , G. w. , 1940, Age of the S::hooley peneplain: .we rica.I1 Journal of Science , v. 2�8, p. 461-476 . Concludes that only one peneplain was formed in post-Paleozoi· time in the Appalachians ; that this peneplain (Schooley) passes beneath the cretaceous sediments of the �oastal Plain at the Fall zone and is the same as the "Fall Zone" peneplain; that it was formed chiefly in Jurassic time; that it was not greatly uplifted and subjected to effective erosion until mid-Tertiary time; that remnants still exist on tops of the mountains .

Stose , G. W. , and Miser, H. D. , 1922, Manganese deposits of western Virginia : Virginia Geological Survey Bulletin, v. 23, 206 p. Physiography section is worthwt,ile .

Stose , G. w. , Miser, H. D. , and Katz , F. J. , 1919, Manganese deposits of the wesc foot of the Blue Ridge , Virginia: Virginia Geological Survey Bul letin,

'' o 171 166 P• Physiographic forms section is ·�rthwhile .

Stose , G. w. , ana Stose , A. J. , 1951 , Blue Ridge front - a fault scarp: Geological Society of America Bulletin, v. 62, p. 1371-1374 . A comment on White's 1950 article of the same name . �ey argue tha t there is no evidence of faulting cJ id that Davis's 1904 explanat1on, tha t the scarp is produced �1 the Atlantic dra�nage working its way back into the Gulf drainage . is the best .

Stout , W. , and Downs , S. , 1931 , The Minford silts of southern Oh io: Geological Society of America Bul letin, v. 42 , p. 663-672 . ConcJ udes that the pending was caused by the invasion of early drift sheets; that the fine-grained, laminated silts of the Minford type were derived from the schists of the Piedmont ; that the new drainage lines were established simply by the ponded waters pouri�g over low cols �� d divides; that the new stre� flowed undisturbed until they had cut youthful valleys nruch below the former drainage level, and tha t the etfects of the later r: linoian and Wisconsin sheets were only to fill the new drainage �ays with some 100 ft or more of 01;twash .

Stout , w. E. , and Lamb, G. F. , 1938, Physiographic features of southeastern Ohio: Ohio Journal of Science , v. 38, p. 49-83 . Discusses monadnock hills representing possible remnants of original surface ; Ha rrisburg penep!ain; Lexington peneplain; Parker strath with Teays , Pittsburgh, and Dover drainage systems developed ; Deep stage drainage , with Cincinnati , Newa rk , an� Pome roy drainage developed; Post-Illinoian drainage ; present drainage .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Strahler , A. , 1969, Forest ecology of the Fai rfax Lin� , Virginia and West Virginia [Ph.D. thesis): Baltimore, Johns Hopk ins University, 126 p. Present forests may be divided into map units which are based on the presence or absence of selected woody species and which are di stinct from both floristic and statistical points of view. The units show a pattern of alternation with topography which is repeatable and predictable . The alternatio�s vary from rock type to rock type , and are probably best explained by variations in substrate moisture related to topographic form.

Strahle r, A. N. , 1944, Regional superposition on the Schooley peneplane : American Journal of Science , v. 242, p. 563-567 . Attacks Von Engeln's hypothesis that northern Appalachian drainage developed by regional superposition of consequent southeast flowing streams from a coastal plain cove r mantling the Schooley peneplain. Three lines of evidence opposed to this date of superposition, but supporting Johnson's theory of superposition on the older Fall zone peneplain, are 1) the absence of windgaps along some supposed former consequent stream courses but the presence of aligned groups of windgaps well preserved along others, 2) the pres�nce of shallow ridge crest sags into which watergaps have been incised, and 3) the remarkably e" '�n marqin of the inner coastal plain.

Strahler, A. N. , 1945, Hypotheses of stream development in the folded Appalachians of Pennsylvania: Geological Society of America Bulletin, v. 56 , p. 45-88 . Discusses 4 hypotheses of the origin of southeast-flowing st�eams in the valley and Ridge of Pennsylvania: 1) deve lopment of subsequent streams along transverse faults; 2) southeast-flowing Permian consequent streams , modified throughout a long erosion history; 3) progressive piracy and local superposition; 4) regional superpositlon. Dismisses all but the last as viable hypotheses.

Strahler, A. N. , 1946, Elongate intrenched meanders of Conodoguinet Creek , Pennsylvania: American Journal of Science , v. 244 , p. 31-40. This and certain other streams of the Martinsburg shale belt h1ve elongate intrenched meanders in which bends of small radiu5 are connected by long, straight, stretches whe re the stream flrJWs transverse to the shale strike. This peculiar meander fnT!:l :.s attributed to greater ease of lat�ral cocrasion where stream flow is parallel to steeply dipping slaty cleavage plates than where stream flow is transverse to the plates . This has resulted in outward growth of meander bends without marked increase in radius of curvature, which in turn has gceatly delayed cutoffs.

Strahler, A. N. , l952 , Hypsometric (area-altitude ) analysis of erosional topography : Geological Society of America Bulletin, v. 63 , p. 1117-1142 . Mainly a t�chniques pa�r, but presents hypsometric curves for areas in the Virginia Piedmon� , the Great Smoky Mountains, the Ozark Plateau, and Alabama Interior Low Plateau.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Straw, H. T. , 1940, The relative relief of the Eastern Highl�nd Rim Plateau of Tennessee ; a study in the cartographical presentation of surface configuration: Tennessee Academy of Science Journal , v. 15, p. 372-380. Presents and de scribes map of relative relief of entire Highland Rim of Tennessee in terms of 200-ft intervals.

Stringfield, V. T. , LeGrand , H. E. , and LaMoreaux, P. E. , 1974, Karst and paleohydrology of carbonate rock terranes in semiarid and arid regions with a comparison to humid karst of Alabama : Alabama Geological Survey Bul letin, v. 105, 106 p. Pages 19-37 discuss karst in Alabama . Most of the bulletin is about karst in arid regions.

Stringfield, v. T. , and Smi th, R. c. , 1956, The relation of geology to drainage , floods , and landslides in the Petersbu rg area , West Virginia: West Virginia Geological and Economic Survey Report of Investigations, v. 13, 19 p. During the rains on June 17 , 1949 , several landslides occurred on the steep dip slopes of the Tuscarora Sandstone on the east side of the Wills Mountain anticline which forms North Fork and New Creek Mountains . One slide temporarily changed the cour£e of the North Fo rk . The topography indicateb that such slides have occurred in the past. Re striction due to a water gap makes floods more seve re in the area .

Stuckey, ,J. L., 19155, North Carolina: Its geology and IILneral resour.::es: Raleigh, NC, N.C. Dept . of Conserva . and Devel ., 550 p. Pages 7-20 give brief descriptions of the phy& !c�raphic provinces in North carolina.

Suess, H. E. , 1954, •· S. Geological Survey radiocarbon dates I: Science , v. 120 , p. 467-473. Greater-than 30, 000 yr radiocarbon date reported for peat �j muck below J� ft of colluvial sediment in Cleveland County , N.C.

swadley, w. c. , 1971 , The preglacial Kentucky River of nort.'1era Kentucky: lJ .S. Geological SUr�ey Professional Papc:r, v. 750-D, p. Dl2 7-ul31. An abandoned high-level river valley extends from the Kentucky River near Carrollton, KY, northeast to the ncuth of the Great Miami River at Lawrence�rg, Indiana, a di ftance of about 40 rni. The geographic location, gradient, ard fluvial-sedi�nt content of this valley identirt it as the pre9lacial course of �� e Kentucky River . It fall�� closely the Ohio River valley but only locally coincides with it. Glaciation reversed the flow of this part of the ancestral Kentucky River and establ ished the course of the Ohio River Jownstream from Lawrenceburg . Glacial deposits filling th-:! preglacial valley probably prevented the nP.Wly formed Ohio Rive r from occupying most of the old valley.

swadley, w. C. , 1977, Geologic rnap of pdrt of the Bethlehem Quad rangle , Trimble and Oldham counties , Kentucky [Map] : u.s. Geological surve:y Geologic �J adrangle Map, v. GQ-1436 , 1 p. Map shows glacial outwash (along Ohio R'ver) and gla�ial drift in northern Kentucky. Dr ift is divided into 3 type s based on degree of weathe ring and topographic position (but not mapped separately).

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Swadl ey, W. C. , 1977 , Geologic map of the Bedford quadrangle , north-central Kentucky [Map) : U.S. Geological Survey Geologic Quadrangle Map , v. GQ-1409, 1 p. Map shows old glacial drift in northern Kentucky. Drift occurs mostly as thin irregular caps on ridges and locally as thicker bod�es that seem to be remnants of deposits that filled preglacial valleys .

Swadley, W. C. , 1980 , New evidence supporting Nebraskan age for origin of Ohio River in north-central Kentucky: U.S. Geological Survey Professional Paper, v. 1126-H, p. Hl-H7 . Glacial deposits at 4 localities in north-central Kentucky sup port a Nebraskan age for the origin of the Ohio River drainage system. These deposits, including till and outwash , are deeply weathe red and must be as old as Kansan . They occur in valleys that deeply dissect the pre-Pleistocene Madi son divide and that were carved by the Ohio River and its tributaries during a long period of erosion. Thus the glacial diversion that disrupted the Pliocene drainage and created the Ohio River substantia!ly preceded the Kansan Glaciation and must have occurred during the Nebraskan Glaciation .

Swingle , G. D. , 1959, Geology, mineral resources, and ground water of the Cleveland area, Tennessee : Tennessee Division of Geolog}· PJlletin, v. 61, 125 p. Pages 38-42 discuss gravel and colluvial deposits. Distinguishes 3 levels of gravel s. Pages 55-57 discusses erosion surfaces and the relation between erosion surfaces and the unconsolidated deposits .

Swinnerton , A. C. , 1929, Changes in base-level indicated by caves in Kentucky and i>emuda [Abstract): Ge•Jlogical Society of America Bulletin, v. 40 , p. 194 . Hypothesizes that systems of caves can not develop beneath regional baselevel ; that lowest levels of systems of caves approximate the baselevel of the region at the time the cave rns were excavated . says that , in Mammoth cave , the continuous system of caverns at approximately 200 ft above the level of the river is so strongly marked that it may be regarded as indicating an intermediate �rosional stage in the physiographic history of the regi�n.

Tanner, w. F. , 1956, Parallel slope retreat in humid climate� : American Geophysical Union Transactions, v. 37, p. 605-607 . Measurements on 1:24, 000-scale topographic maps of northern Alabama suggest the following: 1) streams in v- shaped valleys are flanked by convex-upward slopes ; 2) slopP.s above pediments , valley strip� , or floodplains are lower than the slopes above actively downcutting streams ; and 3) slopes above pediments , valley strips , or floodplains retreat at essentially constant angles .

Ta rr, R. s. , 1898 , The peneplain: American Geologist, v. 21 , p. 351-370 . Attacks Davis's peneplanation concept , using some examples from the Appalachians . Proposes the alternate hypothesis of beveling down to mature form - notes that to reduce a mountainous region to the stage of maturity is an easy task compared with the reduction of a mature mountain region to a peneplain.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Tarr, w. A. , 1924, Intrenched and incised meande rs of some streams on the northern slope of the Ozark PlateaJ in Missouri: Journal of Geology, v. 32, p. 583-600 . Hinkson Creek began its incisement much later than the rivers to the south began to intrench themselves , and has developed its meande rs through lateral and downwa rd cutting, thus producing "i.ncised meande rs" with "slip-off slopes" on the upland spurs . In contrast are the "intrenched" meande rs of the rivers to the south , caused by simp.te downward cutting. The incised meanders of the Hinkson are due to static rejuvenation (caused by the downwa rd cutting of the parent stream, the Missouri ), and the intrenching of the Osage , Gasconade , and Me ramec rivers is due to the upl ift of the entire area, which probably occurred in late Pl iocene times.

Tedrow, ,J . D. F. , and MacClintock, P. , 1953 , Loess in New Jersey soil materials: Soil Science , v. 75, p. 19-29 . Thinks some of the soil material norL� �1d nor��east of Trenton , as deep as 10 ft but more commonly 2-3 ft, is loess .

Teeri, J. A. , and Smi th, A. P., 1971, Active stone polygons on Bluff Mountain, No rth carolina: Journal of the Elisha Mitchell Scientific Society, v. 87 , p. 124-126. Active patterned ground occurs on Bluff Mountain, NC, at 1,380 m elevation. Individual polygons range from 10 to 40 em in diameter and are located along a bog margin in a large , shallow valley near the mountain sunmit.

Teller, J. T. , 1973, Preglacial (Teays ) and early glacial drainage in the Cincinnati area, Ohio, Kentucky, and Indiana : Geological Society of America Bulletin, v. 84 , p. 3677-3688 . Proposes and discusses a history of drainage evolution for the Cincinnati area .

Teller, J. T., and Last , w. M. , 1981, The Claryvi lle Clay and early glacial drainage in the Cincinnati , Ohio, region: Palaeogeography , Palaeoclimatology, Palaeoecology, v. 33, p. 347-367 . The Claryville Clay is lacustrine .;ediment that has bt.�n �reserved in an entrenched meande ring valley beyond the maYimum extent of glaciation SE of Cincinnati . Although the Clartville is pre-Illinoian in age , its "normal" remnant magnetism t>uggests that deposition occurred within the past 700 , 000 yr or so . Present-day rivers lie more than 50 m below the floor of the abandoned Claryville River valley.

Tew, K. H., 1981, A quantitative geomorphic investigation of the pre-cretaceous erosion surface beneath the inner Coastal Plain of North Carolina [M.S. thesis ]: Raleigh, NC, North ca rolina State University, 40 p. well logs were used to reconstruct basement topography in sufficient detail to permit some recognition of baseme1 ': drainage patterns and interpretation of the history of the buried surface . In the study area , basement topography is more sillll.lar to that of the present Piedmont than to that of the Coastal Plain. Fig. 4 is topographic map of basement surface, and Fig. 5 shows longituninal profiles of basement valleys .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Tewalt, S. , 1966 , Fluvial terraces of part of the South Branch Potomac Rive r [M.S. thesis] : Morgantown ,WV, University of We st Virginia, 87 p. Mapping at a scale of 1:62 ,500 distinguished the floodplain and 3 terrace fami lies . The A2 and A3 deposits may have originated c.s channel deposits, whereas AO and Al may be ove rbank deposits. A total of 15 samples were collected from these terraces and tested in the laboratory to determine if the groups could be differentiated by physical and chemical cha racteristics. Particle-size, heavy-mineral analysis , a�d x- ray diffraction of cl ay minerals were carried out. Cluster analysis indicated distinct differentiation between groups . Soil profile development and soil characteristics were useful for separating AO from the terraces.

Thomas , P. C. , 1973, Probable rejuvenation of the Piedmont in the James River drainage basin [M.S. th�sis): Chapel Hill, NC, unive rsity of No rth carolina , 66 p. The Piedmont is often cited as an example of a dissected peneplain. The Piedmont sect;on of the James River drainage basin in Virginia was examined by parallel profiles, divide envelopes, gene ralized contours, and valley profiles to evaluate any erosion surface and possibla rejuvenation . This area does not show widespread or clear evidence of former erosion levels or plane-like surfaces. It shows no features such as large paired terraces or significant knickpoints in stream profiles. Breaks in slope indicate rejuvenation of a surface of mode rate , often geologically controlled relief. This rejuvenation has been pervasive , but apparent stream incision decreases systematically away from the James River.

Thompcon , H. D. , 1936, Hudson gorge in the Highlands : Geological Society of America Bulletin, v. 47, p. 1831-18�8 . Argues that Appalachian drainage evolution is best explained by headward erosion of Atlantic-slope streams ; i.e., most present streams are subsequent in origin. The Hudson is the most successful of the many originally small Atlantic-slope stre�s that were competing for drainage of this part of the Highlands . Because of a favorable location along weak-rock belts and a shorter distance to the sea, it was able to work headward through the Highland. Suggests that more pronounced eastward-tilting of the Atlantic border, and narrower outcrops of crystalline rocks, could account for the greater success of the Atlantic-slope streams of the north as compared to those of the south .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Thompson , H. D., 1939 , Drainage evolution in th€ southern Appalachians : Geological Society of America Bulletin, v. 50, p. 1323-1356 . How the Appalachian drainage was reversed and the divide shifted to :. ts present position has long been a major question of Appalachian geomorphology , commonly answered by regional superposition. Suggests an alternative interpretation: Headwater piracy along the asymmetrical wa tershed resulting from eastwa rd tilting of the Atlantic border region can account for the westward migration of the main drainage divide . Thus the process of drai�.ge reve rsal has been slow and long-continued rather than abrupt . In the N part of the southern Appalachians , the relations of streams to rock resistance and structure , the characteristics of dry gaps , the drainage of canoe-shaped valleys, examples of recent and imminent piracy , and the present asymmetri:al position of the divide support this int�rpretation.

Thompson , H. D. , 1941, Topographic analysis of the Monterey, Staunton, and Harrisonburg quadrangles: Journal of Geology, v. 49, ?· 521-549. calculation of altimetric and hypsometric curves leads to the following conclusions: _) within the �imits of •1eak rocks, the Harrisburg peneplain is well developed in the Harrisonburg quad , more poorly in the others; 2) no peneplain above thr; Harrisburg i.s evidenced by the methods used here ; 3) considering the close :elationship between topography and bedrock , the present topography can be satisfactorily explained without recGurse to former planation of weak � resistant rocks alike .

Thompson , H. D. , 1919 , Drainage evolution in the Appalachians of Pennsylvania: New York Academy of Sciences Annals, v. 52, p. 31-62 . Says the southeastv1ard drainage can be accounted for by

normal processes of headwater piracy along an asymmetric divide •.• the originally west-flowing streams have been reversed from west to east - In thi s manner, the main watP.r�;hed has slowly migrated westward from its early location to its present position in the Plateau . Replies to Strahler's objections to his 1939 paper. Stresses adjustment of streams to structure ru1d lithology.

Thompson , H. J., 1969, The James River flood of At•gust 1969 : Weatherwi se , v. 22, p. 180-183. Puts the re�1rrence inte,val of the storm at greater than �.ooo yr. Notes that a rare cnmbination of factors interacted to produce an exceptionally high magnitude of conceHtrated rainfall; these factors are discussed.

Thompson , M. L., Smeck , N. E., and Bigham, J M. , lSSl, Parent materials and paleosols in the Teays River valley, Ohio: Soil Science Society of America Journal, v. 45, p. 918-925. Paleosols were developed in materials unde rlying the loess (i.e., colluvium or alluvium) . More intense mi. neral weathering in the paleosol compared to overlying or unde rlying ho rizons was indicated by its higher ratios of mica weathering products to mica ln the clay fractions , higher exchangeable Al, arn lower K/Z r values in the fine silt fraction.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Thompson, P., �chwarcz, H. P. , and Ford, D. C. , 1976 , Stable isotope geochemistry, geothermometry, and geochronology of speleothems from We st Virginia: Geological Society of America Bulletin, v. 87, p. 1730-1738 . Soe1eothems from two caves record relative fluctuations in climate during the period frOQ 200 , 000 yr B.P. to present . Secular variations in the oxygen isotopic composition of calcite in these deposits are largely the result of tempe rature-dependent changes in the isotopic fractionation between calcite and water and are only seconda rily a result of changes in delta-018 of drip wa ters from which the speleothems wL re deposited. The delta-o18c data, taken together with de1ta-Q18w values inferred from fluid-inclusion hydrogen isotope studies , suggest that du ring extreme glacial condi tions , temperatures in these caves fell to at least 0 degrees Celsius, resulting in cessation of deposition. Gaps in the depooitional record, such as from about 40,000 to 4,000 yr B.P. , may correspond to such a cool period.

Tho rnbury, W. D. , 1965, Regional geomorphology ot the United States: New Yo rk , Wi ley, 609 p. Chapters 4-11 summarize geomorphology of Appalachian region as unde rstood to 1964 .

Thorne , R. F., and Cooperrider, T. S. .. 1960 , The flora of Giles County , Virginia: C'stanea, v. 25, p. 1-53 . Provideb a catalog of vegetation in Giles County , complete with key to collecting stations. Mainly a list of plants .

Thorson , R. M. , Clayton , w. s. , ar.d Seeber, L. , 1986 , Geologic &vidence for a large prehistoric earthquake in eastern Connecti�!�: Geology, v. 11, p. 463-467. Postglacial wedges r:tJtting stratified late Quaternary glacial deposits have been widely reported throughout the northeastern IL �.

Think previous int,.. :pre':dtion of these features as periglaci- • ice-wedge casts incorrect. At study site the wedges contaic· material injected from below as well as collapsed from the .>icie . Interpret wedges as extension and collapse fissures that se ·J.lc' a>; conduits for water and liquefied sediment during one or mor! prehistoric lique faction events, probably r.rehistoric earthquc. :

Thrailkill, J. , 1968, Chemical a:� hydroloqic factors in the exr:�vation of limestone caves: Geological Society of America Bul letin, v. 79 , p. 19-46 . In an area where no water crosses the water table, flow in the aquifer will be nearly horizontal and water from sources adjacent to the area will follow shallow flow [o ths . If such water is unde tsaturated with respect to calcite, caves will be excavated . Mammoth Cave was probably formed by unde rsaturated water spi lling from an impermeable bed . After reachiflg the wa ter ti' Jle , tl".is water followed shallow-phreatic paths in the area beneatl" the impermeable bed . Backflooding from the G:P.Pn River may have aided in the excavation cf the cave .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Thrailkill, J. , 1984 , Hydrogeology and envi rvnmental geology of the Inner Bluegrass karst region: Field guide for the Annual Meeting of the Southeastern and North-central Sections , Geological Society of America, Lexington , KY, Ap ril 4-6 , 1984: Lexington , KY, UnivP.rsity of Kentucky, 31 p. Field guide de�cribes Joyland Cave , Newto� swallet, Mallory sink road cut .:.hawing shallow solutional features, and Royal Spring. TOpics discussed fer each: Description dnd envi ronmental hazards , hyd rogeology, g1ology .

Thrailkill , J., 1985, The Inner Blue Grass region, in Doughe rty, P. H. , ed ., Caves and karst of Kentucky: Ken . Geol . Surv . Sp. Pub. 12, Ser . XI : Lexington , KY, Kentucky Geological Survey, p. 28-62 . Discusses groundwater basins , structural and lithologic control of groundwater flow, sinkhole origin, types of subsurface flow, conduit initiation and stages of growth, and influence of human activit::.es.

Thrailkill, J., Byrd , P. E. , Hopper, W. H. , Jr., McCann, M. R. , Spangl er, L. E. , Troest�r, J. w. , Gonzie , D. R. , and Pogue , K. R. , 1981 , The Inner Bluegrass karst region, Kentucky, in Beck , B. F., ed ., Eighth International Congress of Speleology Proceedings : Huntsville, AL, NSS , p. 336-338 . Discusses delineation of ground-water basins by means of dye t.acing. 'lhe typical major ground-water basin has an area of about 20 square kilometers. In some areas where karst features are not !ihown on the map, much of the drainage is unde rground th-:ough stream-bed swallets, while in other such areas (which are often on subsurface divides ) there is little subsurface drainage and many of the groundwater basins are thus individual karst aquifers.

Tierney, J. , 1985, Caves of northeastern Kentucky (with special emphasis on Carter Caves State Park ), in Doughe rty, P. H. , ed., Caves and karst of Kentucky: Ken . Geol . Surv. Sp. Pub . 12, Ser. XI : Lexington, KY, Kentucky Geological Survey, p. 78-85. Describes features in Carter caves .

Tig�t, w. G. , 1897 , Some preglacial drainage features of southern Ohio: Denison University Bulletin, Journal of the Sci . Lab. , v. 9, p. 22-32 . Discusses drai•�ge features that appear to antedate the onset of glaciation : some futures of the Ohio River val ley, the Big Sandy valley of Kentucky ·�ere it enters the Ohio, the California valley from Sciotoville to Wave rly, the Symmes Creek and Salt Creek va lleys , the correlation of drainage and topographical features, and a pseudoccl .

Tight , w. G. , 1903 , Drainage IOOdifications in southeastern Ohio ana adjacent parts of west Virginia and Kentucky: u.s. Geological Survey Professional Paper, v. 13, 111 p. Very useful study . Includes sections on old high-level valleys , Teays valley, Hurrican3 Creek drainage , drainage modifications , historical relations of the old high-level drainage system to the present . Good maps .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Torbett, C. A. , and Clark, G. M. , 1985, Morphology, pedology, and origin of selected sorted patterned gro��d , Great Smoky Mountains National Park , Tennessee/North Ca rolina [Abstract ): Geological Society of America Abstracts with Programs, v. 17 , p. 137. Describes patterned ground on SE side of Rocky Top . Sorted stripe ; 3-10 rn wide extend 150 rn and coalesce with reworked material along an incised drainageway .

Tormey, B. B. , and Petersen, G. w. , 1982 , Classification of soil and sediment characteristics on geomorphic surfaces of the Falls stretch of the Potomac Riv�r using R- and Q-mode factor analysis [Abstract ): Geological Society of America Abstracts with Programs, v. 14, p. 91 . 36 soil ar.d sediment variables were measured at 38 sites . Q-mode factor analysis clustered these 38 soils into 5 distinct groups : 3 groups representing a modern floodplain catena , and 2 groups mantling preglacial Pleistocene terrace levels above the 100-yr flood. Two types of variables used: sedimentary variables related to size, shape , and provenance , and soil development VdriaLles characterizing soil color, mottling, and clay illuviation. Higher soils had greater concentrations of coarse fragments and better developed clay bulges .

Touysinhthiphonexay , K. c. N. , and Gardne r, T. w. , 1984, Threshold response of small streams to surface coal mining, biturnimous coal fields , central Pennsylvania: Earth Surface Processes and Landforms, v. 9, p. 43-57 . Stream response to increased discharge and channel shear stress produced by increased surface runoff from regraded mine spoil takes the forms of enlarged c�;nels and increases in the size of moving blocks. Where peak discharges and associated shear stresses exceed the c03bined etosional re$istance of floodplain vegetation, collullial blocks, and channel banks, streams adjust extensivel�' to higher levels of mining, :ausing an abntpt increase in the si<::'! of transported blocks and eroded channels. In the first-order basins studied, this stepped re.;ponse occurs at approximately 0. 45 square kilometers mined area and 50 percent of the total basin area mined . For streams that have exceeded �th threshold levels, disequilibrium is demonstrated by a strong positive correlation between local stream slope and basin area.

Trainer, F. w. , and Ellison, R. L., 1967 , Fracture traces in the Shenandoah Valley , Virginia: Photogrammetric Engineering, Feb. , p. 190-l99. Fracture �races seen on aerial photos are interpreced as the surface expression of joints or groups of joints in the bedrock . Differences between the preferred orientation of tht fracture traces and that of the joints in these folded rocks are therefore attributed to selective formation of the traces along only the ve rLical joints . The dip of the strata is beli eved to control the acrundance of fracture traceG because both vertical joints and fracture traces appea r to be more numerous in gently dipping strata . Table 2 shows abundance of fracture traces i� different stratigraphic unit�.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Trimble, s. w. , 1970, The Alcovy River swamps : The result of culturally accelerated sedimentation: Georgia Academy of Science Bulletin, v. 28 , p. 131-141. After European settlement, sediment from erosion of newly cleared and r.oorly f'!rmed uplands soon began to fill the streams . The channels of the main streams had built up enough so that swamping �f some bottomlands was apparent by the time of the Civil Wa r. Because of continued sedimentation and stream aggradation, the area of swamps and marsh has increased through th'" yea.:-s .

Trim.'Jle, s. W. , 1971 , CUlt•:;:.:' ly accelerated sedimentation on the middle Georgia Piedmont: Fo rt Worth, TX, Soil Conservation Service, 110 p. Documents acce:erated sedimentation of stream valleys that occurred following European settlement of thf!! Piedmont . This is also Trimble 's M.A. thesis, university of Georgia, 1969 , 110 p.

Tt imble, s. w. , J.9n, Man-induced erosion on the southern Piedmont of the USA: A perSP£Ctive, in Adams, w. P., and Helleiner, F. M. , eds., International Geography : Toronto, university of Toronto , p. 454-457. Documents damage caused by European agriculture . Much of the bott;:mlanrl was literally buried by less fertile sediment. Of greater agricultural significance was erosion damage to the -..:plands . The �;urficial sandy loam har't been removed from much of th.:- -'i 1ands l.!cNing on!y the clay ::.,-soil or deep gullys . 3;11 ... :. ; often tormed canyons in the deep saprolite an.d was a prime so;,:;,·:;e of stream sediment . Whereas the Virginia Piedmont had approximately 10% of the land ruined for agriculture and North caroliP4 had 20�, the southerly area had 40%. In central Georgia, •"' average of l7 em was reDK:Ved from the uplands . As a result of di��Jished erosion and sediment load, l�r order tributaries are r. .:JW ..!egrading. The sediment is now swamping some areas along � larger ;ivers.

Trimble, S. W •• 1974, Man-induced soil erosion on the southern Piedmont , 1700- 1970: Soil Conservatlon Soc . �f America, 180 p. Historical records o= land use were converted to a composite index of erosional int.ensity, called "erosive land use" (ELU) . With this tool it was possible to trace the history of soil erosion on the Piedmont using other data such as stream sedimentation rates and Soil Conservation Service estimates of thickness of the soil profile removed (made for selected areas ) as addi tional evidence . Presents evidence that erosion was negligible in aboriginal times . ELU becare more severe when clean-cultivated crops and slav�ry predomr.c1ted . OVer much of the Piedmont , debris filled streams and covered floodpla\ns. ELU decreased greatly during the 20th century. Because of the resulting reduced stream loads , modern sediment deposits in the headwater valleys of some areas are now being dissected, and the sediment is ooing transported farther down stream.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Trimble, S. W. , 1975, A volumetric estimate of man-induced soil erosion on the southern Piedmont , in Present and prospective technology for predicting sediment yields and sources: u.s.D.A. Agricultural Re s. Service Pub .

S-·40: Houston, TX, U.S. Dept . of Ag riculture, p. 142-152 . Used large-scale surveys in which detailed estimates of average depth of soil removed were made , supplemented with small-sca).e surveyr in which soil had been classified into 1 of 6 categories, from "little or none" to "destroyed by gullying." Figures obtained are much greater than frequently cited denudation rates, but seem reasonable. In large areas of Georgia and South Carolina average depth is greater than 12 inches. The average for S.C. was 9.6 in. Average for entire Piedmont is 7.1 in. In all , more tha' 6.1 cubic m\les of soil are estimated to have been eroded from Piedmont slopes.

Trimble, S. w. , 1975, Denudation studies: Can we assume stream steady state?: Science , v. 188, p. ·_ .:J7-1208. Contemporary stream sediment loads are dubious indicators of r�gional denudation. Recent analysis of 10 river basins in the southeastern u.s. indicates that of the mater�al eroded from upland slopes since EUropean settlement, only about 5 percent has been exported. The remainder, alluvium and colluvLllTl .. will pr.Jbably not be exported because of extensive reservoir impoundments.

Trimble, S. w. , 1977 , The age of the Alcovy swamps : A discussion: Southeastern G�ology, v. 18 , p. 191-194 . A discussion of article by Staheli et al who attackeo Trimble 's 1970 article . Basically, Trimble says that most of the stream sedimentation that resulted from soil erosion took pl�ce in and along the channel. Bottomland quite distant fromthe stream might be covered only by a thin layer of silt and clay. ,ience , the claims of Staheli et al as to the antiquity of the surface of this part of the bottomland is reasonable, but that this doesn't bear on the amount of modern stream deposition that has taken place near the channel.

Trimble, s. w. , 1977 , The fallacy of stream equilibrium in contemporary denudation studies: American Journal of Science, v. 277 , p. 876-887 . Contemporary stream sediment loads are dubious indicators of regional denudation. In many larger basins, sedi ment storage in the form of colluvium and alluvium appears to be much greater tha .. sediment yield. Analysis of 10 large river basins in the southeastern u.s. indicates that while upland erosion was proceeding at about 95 �00 yr , sediment yields were only ?�ut 5. 3 ITill/lOO yr , & delivery ratio o:: dbout 6% . Much of the m..dern erosional debri� is stored in the stream syste� �s massiv� deposits in streams and valleys . Some of these depooit� are presently being eroded and are now themselves Jrcess� of sediment yields. However, the transport of sediment is significantly impeded by extr·nsive reservoir impoundments . Thus , present sediment yields correlate poorly with upland erosional processes or phenomena such as lithology, climate , vegetation , and land use .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Trimble , S. w. , and Carey, W. P. , 1984 , Sediment characteristics of Tennessee streams and reservoirs: U.S. Geological Survey Open-file ReprJrt, v. 84-719, 32 p. Transport C\•rves show that when flow is less than about 1 cfs/square mile, western Tennessee streams ha·.·e higher concentrations than middle or eastern streams. When flow exceeds about 10 cfs/square mi le , however, concentration� in middle and eastern streams can equal or exceed t.'tose in western streams . The more efficient sediment-delivery processes operating in middle and eastern Tennessee basins are responsible for the rapid increases in suspended-sediment concentration wi th increasing flow. Sediment yields for middle and eastern basins generally are les� than 800 tons per square mile per year, a:�though heavily strip-mined basins can have yields from 1,000 to 3,000.

Troestler, J. w. , White, E. L. , and White, w. B. , 1984 , A comparison of sinkhole depth frequency distributions in temperate and tropic karst regions , in Beck , B. F. , ed ., Sinkholes : Their geology, engineering and environmental impact - Proc. of the First �u ltidisciplinary Conf . on Sinkholes, Orlando , FL: Rotterdam, Balkema , r 65-73. Ta.e frequency of OC-"Urrence of sinkholEs decreases exponentially

�ith depth following the equation N • NU e �aised to the power -Kd, where NO and K are constants. The K coeffici�nt ranges from 0.22 to 1.19 m-1 in temperate karst regions , where 1t is unaffected by litholgy or structure . It is different from tropical regions . The inverse of K gives a characteristic depth tor each population of sinkholes. The characteristic depth of dolines in temperate regions ranges from 0.85 � in Florida to 4.5 m in the Appalachians . In tropics, much greater. Deline density is also discussed.

Troutt, R. w. , 1971, An occurrence of large scale , inactive , sorted patterned ground south of the glacial border in central Pennsylvania [M.S. thesis]: University Park , PA , Pennsylvania State university, 71 p. A detailed description of &orted nets and boulder concen trations. Area is entirely underlain by Tuscarora . Dug trench, did large-scale mapping, measured block orientations , and attempted to observe block movement by painting a straight line across slope in two areas .

Tschudy , R. H. , 1965, An upper Cretaceous deposit in the Appalachian Mountains : U.S. Geological Survey Professional Paper, v. 525-B, p. B64-B68 . Used palynology to establish uppe r Cretaceous age of lignile usPd by Pierce to demon�trate a Cretaceous age for some residuum.

u.s. Geological Survey, 1970, National atlas of the united States; washington , DC, u.s. Geological Survey, 417 p. Of special interest are P.elief (p. 56-58 1, Physj ngraphy (p. 59 i, Phys iographic Di•·i.sio.,s (p. 60 ), Land-surface Form (p. 61··64 ),

Glacial geology , I?· ·, �; ), and Kustlands and Cave ::ns ( p. 77).

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 u.s. Geological Survey, 1977, Preliminary report on Belair exploratory trench no. 10-i6 near Augusta , Georgia: u.s. Geological Survey Open-file Report , v. 77-411, 20 p. Detailed de scription of trench dug across Belair fault zone , including diagrams .

u.s. Geological Survey, 1982, Goals and tasks of the landslide part of a ground-failure hazards reduction program: U.S. Geological Survey Circular, v. 880, 49 p. Four parts: 1) history and scope of problem; 2l process and prediction studies; 3) landside-hazard mapping and d&k evaluation; 4' transfer and use of landslide-t�zard information. Fig. 1 shows relative potential of different parts of u.s. to landsliding; Fig. 16 is example of landslide-hazard map.

Van Tassell, J. , and Grant, w. H. , 1980, Granite disintegration, Panola Mour.tain, Georgia: Journal of Geology, v. 88, p. 360-364. Biotite-induced disintegration of granite fragments in the soils of plant communities on slopes of Panola Mountain proceeds rapidly during early stages of plant succeEsion. Complete disintegration of SOirJI> fragments may take over 670 yr. 'lhe grain size of the minerals in the soils is strongly influenced by tha size distribution of the minerals in the parent rocks.

Van der Schalie, a. , 1939, Distributional studies of the Naia as related to geomorphology: Journal of Geomorphology, v. 2, p. 251-257 . Attacks the idea that birds can transport fresh-water mussels from one drainage basin to another. Notes that perhaps the strongest evidence against this is that most species of mussels have a definite and characteristic geographical distribution pattern within one or more of the major drainage systems, which would not be likely if mussels were haphazardly carried about by birds .

VanArsdale, R. B., 1986, Quaternary displacement on faults with�n the Kentucky River fault system of east-central Kentucky: Geological society of America Bulletin, v. 97 , p. 1382-1392 . Numerous faults of KRFS (Kentucky River fault system) are partially overlain by Pliocene-Pleistocene terrace sediments along the Kentucky River. Preliminary drilling and electrical resi�tivity surveys suggest that a mmber of the faults have been act ive sin::e the deposition of the terraces. From these preliminary surveys , 9 trenches were excavated. Four of these revealed faulted and/o r folded terrace sediments. one trench revealed a reverse fault which displaced terrace seds 0.7 m. Believes folding and faulting of the terrace deposits is tectonic in origin and has been active within the past 5 m.y. and probably within the past 1 m.y. Good cross sections.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Va rnedoe , w. w. , Jr., 1963, Cross pi racy drainage d&velopment in the Newsome Sinks area of Alabama : NSS Bulletin, v. 25, p. 83-87 . In th� Newsome Sinks area of Morgan County, Alabama, a young surface stream cut across and down into an older , underground drainage system that formerly resurged at Skidmore Cave . As a result each captured the drainage of the other. The present alignment of the caves in the area, the Newsome Sinks water resurgence at Hughes Spring and the resurgence at Skidmore Cave can best be explained by this history. Newsome Sinks is today a large landlocked valley containing no surface streams and nume rous caves. Diagrams illustrate proposed drainage changes.

Velbel, M. A. , 1985, Geochemical mass balances and weatherin�. rates in forested watersheds of the southe rn Blue Ridge : American Journal of Science , v. 285, p. 904-930. Weathering rates of rock-forming silicate minerals in natural forested watersheds can be calculated using a system of geochemical mass balance equations constructed and constrained by petrologic, mineralogic, hydrologic, botanical , and aqueous geochemical data . Solving the systems of equations for the weathering rates of biotite mica, almandine garnet , and oligo=las�·�esine plagioclase feldspar in saprolitized schis�� and gneisses of Coweeta Lab indicates that the rate at which the weathering front penetrates into fresh rock is 38 mmv1000 yr, which agrees well with the average denudation rate for the southern Appalachians .

Velbel, M. A., 1985, Hydrogeochemical constraints on mass balances in forested watersheds of the southern Appalachians, in Drever, J. I., ed ., The chemistry of \o.'eathering: Reidel Pub. Co ., p. 231-247. TWo variables, parent rock type and flushing r�te, control the long-term dissolved load of streams in the forested watersheds . The same variables explain qualitative stability relations, as shown by stability field diagrams which are, in turn, consistent with the hydrclogy and kaolinit�gibbsite clay mineralogy of the profiles. The consistency of hydrology, aqueous geochemistry and clay mineralogy places useful constraints or1 more sophistocated geochemical mass-balance models.

Velbel, M. A. , 1987, Alluvial fan origin for terrace deposits of the southeast Prentiss quadrangle, near Otto , North Carolina: Southeastern Geology, v. 28, p. 87-103. Lithologies and structures in unconsolidated terrace gravels, sands, and silts formerly exposed along u.s. Highway 23-441 near Otto, NC, suggest deposition on an alluvial fan . OUtcrops showed laterally extensive sheets of massive, poorly sorted, matrix-supported conglomerates interbedded with channel-filling cross-bedded sands, and tabular sheets of homogeneous or poorly plane-laminanted fine sands and silts. One paleosol with a prismatic structure strongly reminiscent of n�tric horizons of arid alluvial soils was observed.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Velbel , M. A. , and Grantham, J. H. , 1985, Depositional models for Te rtiary Quaternary terrace deposits of the southeast Prentiss quadr�,gle, Macon County, No rth Carolina [Abstlact]: Geological Society of America Abstracts with Programs, v. 17 , p. 140. Sedimentary and pedogenic structures in unconsolidated terrace deposits exposed along U.S. Highway 23-441 in the southeastern Prentiss quad suggest alluvial fan and fluvial environments of deposition. Interprets coarser deposits as sheet-flood, fluvial channel, and flood-plain deposits on laterally overlapping fans . 'tt1e finer deposits may represent either distal outer fan deposits or deposlts of the ancestral Little Tennessee River. Sediment properties of possible paleoclimatic �ignificance are being investigated in light of the paleosol evidence for an arid episode in the depositional history.

Ver Steeg, K. , 1929, Certain characteristics of peneplanes: Pan-Ame rican GeologiGt, v. 52 , p. 340-342 . Discusses reasons why there roay a�ar to be mere peneplain remnants in an area than there actually are. First, peneplains are not flat; there should be a rise oe the surface toward the divides established by the streams flowing on it. 'lhe tops of the divides on a peneplain surface might be interpreted as an older, highe r peneplain, and the lower slopes as a later, younger one , when in reality, the whole represents cne surface onl·•. Another factor is the thickness of the resistant bed. 'lhe original �neplain may be presered on thick, resistant formations and entirely removed on thin beds of equally resistant rock . The breadth of a resistant formation is also important . Warping or faulting of peneplains may give two or 100re levels that might be intarpreted as distinct surfaces.

Ve r Steeg, K. , 1930, Wind gaps and wate• �aps of the northern Appalachians , their characteristics and significance : New York Academy of Science Annals, v. 32, p. 87-220. Constructed longitudinal profiles along all ridges north of the Great Valley and 26 cross profiles across the Triassic Lowland , the Highlands in NJ , the Great Valley, and the Valley and Ridge . Results indicate that wind-gap elevation and peneplanation have no relation. Wind gaps occur at all elevations and are so irregularly distributed that it is certain that no accordance in their levels due to peneplanation occurs anywhe re in the region. 'lhe angle of slopes of the water gaps is mu-.::h steeper than that of the wind gaps .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 VeL Steeg, K. , 1930, Some features of Appalachian peneplanes: Pan-American Geologist, v. 54 , p. 17-28. The originally undulating character of a peneplain may lead one to the erroneous conclusion that the surface has been unequally warped. Monarl.,ocks and stream-divides, especially such as would occur on a peneplain as thoroughly base-leveled as the Schooley (Kittatinny) , might easily be misinterpreted as domes produced by unequal warping due to uplift. Provides example from Fridley (1929) of what appears to be warping of the Schooley peneplain, but which may be reasonably interpreted as due entirely to erosion. The fact that these broad domes occur on stream-divides points all the more conclusively to their erosive nature .

Ver Steeg, K. , 1931, Erosion surfaces of eastern Ohio: �an-Ame rican Geologist, v. 55, p. 181-192 . Recognizes the existence of three distinct erc•sion-surfaces in the n0LJhernAppa lachians anu Allegheny Plateau region : the Schooley (Kittatinny) , :>n the ridge crests of the folded Appalachians ; the Harrisburg, on the weak-rock formations in the vall':!ys of eastern Pennsylvania and co-extensive with the upland erosion surface , beveling the Allegheny plateau in Ohio and western Pennsylvania; ar;d a third one , the WOrthington (Lexington ), well developed in Ohio and Kentucky and correlated with the Somerville of eastern Pennsylvania and New J�rsey.

Ver Steeg, K., 1931, Warping of Appalachian peneplains: Journal of Geology , v. 39 , p. 386-392. Because the Harrisburg peneplain has a pronounced slope toward the southeast, it has been believed that widespread warping of that surface took place in the uplifting of the Appalachians . There is reason to doubt this supposed warping, for evidence of it appears to be lacking in eastern Pennsylvania where the surface has its best development. Provides a contour map of a portion of the peneplain in Pennsylvdnia.

Ver Steeg, K., 1932, Erosion surfaces of the Appalachian Plateau: Pan-Ame rican Geologist, v. 58, p. 31-44. Discusses peneplains of the Appalachian Plateau and their correlation with peneplains of the eastern Appalachians .

Ver Steeg, K. , 1932, Map of the Schooley (Kittatinny) peneplain: Journal of Geology, v. 40, p. 557-559 . Presents a contour map of the restored upper peneplain represented by the even crest-lines of the folded Appalachians in eastern Pennsylvania .

Ve r Steeg, K. , 1933, Windgaps and erosion surfaces: American Journal of Science, v. 226, p. 507-511. Discusses 1933 article by Hickock who claimed that elevations of windgaps correspond to erosion surfaces, contrary to findings of Ve r Steeg in 1930. Ver Steeg says that the large numbe r of erosion surfaces postulated by Hickock and the few windgaps at these horizons makes the validity of Hickock's conclusions doubtful .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Ver Steeg, K. , 1940, Correlation of Appalachian peneplanes: Pan-Ame rican Geology, v. 73, p. 203-210. Tries to prune down the number of postulated peneplains in the Appalachians by correlating some of the peneplains previously held to be distinct surfaces.

Ve r Steeg, K. , 1940, The formation of watergaps by solution and piracy: American Journal of Science , v. 238, p. 32-�1 . This is a response to article by Fridley, 1939. Attacks the hypothesis that the course of the South Branch Pot�mac River through the Smoke Hole in eastern West Virginia is explained by stream pi racy brought about by underground solution of limestone . Says that there is little evidence to support the importance of this process in the formation of watergaps or windgaps in the Appalachian ridges.

Ver Steeg, K. , 1940, Geomorphology of the Catoctin belt: American Journal of Science , v. 238, p. 685-709. Attacks Keith's (1893) concept of the Weverton peneplain and also his proposal of the value of wind gaps as indicators of fluvial baselevel s. Provides table of elevations of wind gaps of the Blue Ridge in order to refute this proposal .

Ver Steeg, K. , 1942, A study in Appalachian physiography : Journal of Geology, v. 50, p. 504-511. G.H. Ashley presented the theory that the present surface in the Appalachians contains no remnant of any of the older peneplains and doubts the existence of more than one peneplain over the whole Appalachian region. The author defends the view that remnants of the Schooley (Kittatinny) peneplain still exist on the ridge crests and uplands throughout the Appalachian and New England region.

Ve r Steeg, K., 1946, The Teays River: Ohio Journal of Science , v. 46, p. 297- 307. Provides a brief ove rview of the course of the Tertiary Teays River, from the Piedmont to the Illinois River.

Viletto, J. , Jr., 1968, Channel morphology in northwestern Pennsylvania [Ph.D. thesis): University Park, PA , Pennsylvania State University, 246 p. Measured the following channel parameters in northwestern Pennsylvania: number and length of channels, drainage density, channel gradients and longitudinal profiles, and confluence angles. Channel density is greater on incised dip slopes than on incised scarp slo:;>es.

Vi rginia Division of Mineral Resources, 1969, Natural features caused by a catastrophic storm in Nelson and Amherst Counties, Virginia: Virginia Minerals, Special Issue , Oct�ber, 20 p. Contains 28 photos and a sketch map with locations of each. Shows many debris avalanches. Slides were most numerous on mountainsides underlain by the Lovingston Formation, a biotite granite gneiss .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Visher, s. s., 1941, Climate and geomorphology: Some comparisons between regions : Journal of Geomorphology , v. 4, p. 54-64. Compares Indiana to areas wi�, different climates with respect to average slvpe , relative abundance of cliffs, badlands , type of sinkholes, and south slope/north slope differences.

Visher, S. S., 1941, Torential rains as a serious handicap in the South : Geographical Review, v. 31, p. 644-652 . Demonstrates how much more common are intense rainfalls in the SOuth than in the North, and discusses probable meteorological causes of this difference .

Visher, s. S., 1942, Regional contrasts in torrential rainfalls help to explain regional contrasts in erosion : Journal of Geology, v. SO, p. 96-10S. In the eastern half of the u.s. there is a general southward increase in the amounts of rain received in short periods. Soil-erosion data from the SCS reveal a general southward increase in erosion upon comparable areas. It is concluded that part of the regional contrasts in erosion can be correlated with the frequency and intensity of hard torrential rains.

Volkes, H. E., and Edwards , J. , 1974, Geography and geology of Maryland : Maryland Geolgical Survey Bulletin, v. 19, p. 36-104, 139-143. Physiography sections provide good introduction.

Von Engeln, 0. D., 1942, Geomorphology: New York, MacMillan, 6S5 p. Chapter 16 , History of the folded Appalachians , on p. 339-368, is a good review of thought prior to 1942. Good diagrams .

Wagner, M. E., and Crawford, M. L., 1975, Polymetamorphism �f the Precambrian Baltimore Gneiss in southeastern Pennsylvania : American Journal of Science , v. 27S, p. 6S3-682. Taconic metamorphism is dated at 440 11rf and a temperature of 6S0-700 degrees C at 7-8 kilobars are deduced . Allowing 3.2 �n burial per kilobar then burial at time of metamorphism was about 24 kilometers. Assuming that erosion and not structural movement has exposed the gneiss at the surface , then the rate of erosion has averaged SO mmv1000 yr since the Taconic orogeny.

Walcott, C. D. , 1893, The Natural Bridge of Virginia: National Geographic Magazine , v. S, p. S9-62. Recogni;.>:ed Hatural Bridge as the remains of a former subterranean pass�gP .

Walcott, R. I., 1972, Late Quaternary vertical movements in eastern North America: Quantitative evidence of glacial-isostatic rebound: Review of Geophysics and Space Physics, v. 10, p. 849-884. Notes crust has not completed its adjustment to the removal of the ice sheet. This revi� collects evidence of ve rtical movements in northern and eastern North America from different sources and disciplines to provide in one pUblication the quantitative data important for geophysical analyses of glacio-isostatic rebound .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Waldrip, D. B., and Roberts, M. C. , 1972, The distribution of slopes in Indiana : Indiana Academy of Science Proceedings (1971), v. 81 , p. 251-257 . Provides slope maps of Indiana prepared by several different methods .

Walters, J. c. , 1975, Origin and paleoclimatic significance of fossil periglacial phenomena in central and northern New Jersey [Ph.D. thesis]: New Brunswick , NJ, Rutgers University, 147 p. By means of field investigation and aerial photographs, the distribution of fossil ice-wedge polygons , boulder fields, congeliturbates, ventifacts, and asymmetrical valleys were studied . Fossil ice-wedge polygons have diameters of 3-30 m. Individual ice-wedge casts range in height f.rom 25-262 em and in width from 10-240 em.

Walters, J. C., 1978, Polygonal patterned ground in central New Jersey: Quaternary Research, v. 10, p. 42-54 . Diameters of the polygons range from 3 to 30 m with an average of about 20 m. The wedges examined in ve rtical exposures range in depth from 25 to 260 em (average , 125 em) and in width from 10 to 240 em (average , 50 em) . The infilling material of the wedges is mostly a sandy loam, although this material is not homoge�.eous throughout the wedges. The presence of ventifacts and frosted sand grains within the wedges indicates eolian activity during the formation of these features. The polygonal ground and wedge structures exhibit several cha racteristics similar to those of ice-wedge casts , and available evidence suggests they way have originated as ice-wedge polygons du ring the last glacial maximum.

Walters, J. c. , 1981 , Valley asymmetry in the Neshanic River basin, west-central New Jersey: Bulletin of the New Jersey Academy of Sciences, v. 26, p. 18- 24 . The river valleys of the Neshanic River drainage basin display a significant valley asymmetry, there being a predominance of steeper north-facing valley sides. It is thought that the asymmetry might have been initially due to the differential effects of insolation in a former periglacial environment .

Ward, F., 1930, The role of solution in peneplanation: Journal of Geology, v. 38 , p. 262-270. Cites 6 pieces of evidence that the Somerville (lowest ) peneplain of eastern Pennsylvania was formed by solution rather than by stream erosion.

Ward, F., 1938, Recent history of the Delaware Valley below the Water Gap: Pennsylvania Topographic and Geologic Survey Bulletin, v. G10 , 76 p. Discusses glacial history and attempts to determine preglacial topography and postglacial erosion.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Watson , R. A. , 1967, unde rground solution canyons in the Central Kent· y Karst, U.S.A. : International Journal of Speleology, v. 2, p. 369-376 . Solution canyons are underground voids 1 to 15+ m wide , 3-45+ m high, and 30 to 300+ m long . Floors are stepped , ceilings level . They occur parallel to and directly unde r the thalwegs of re-entrant valleys tributary to major karst canyons. Solution canyons are related genetically to soluti�nal vertical shafts, forming where removal of the impermeable sandstone caprock permits the vertical descent of water through jointed limestone . Surface runoff concentrates along reentrant thalwegs where a large quantity of water goes underground. This water, plus subsurface water flowing over the caprock breached by the valleys , follows the easiest route to baselevel down major ve rtical joiu�s orlented parallel to the thalwegs .

Watson, R. A. , and White, w. B. , 1985, The history of Americ� · theories of cave origin, in Drake , E. T., and Jordan, w. M. , eds., Geological Society of America Centennial Special Volume : Boulder, CO, Geologicai Society of America, p. 109-123. OUtlines tl� development of thinking on cave d�velopment , touching on caves in the Appalachians. Davis mistakenly attributed most cave genesis to phreatic solution.

watson, T. L., and Cline, J. H. , 1913, Drainage changes in the Shenandoah Valley region of Virginia: university of Virginia Bulletin of the Philosophical Society, Scientific Section, v. 1, p. 349-363. Presents maps showing drainage during different erosional cycles. Hypothesized drainage changes involving captures and wind gaps in the Blue Ridge .

Watson , T. L. , Cline, J. H. , and Harnsberger, T. K. , 1914, Exarupl�s of intercision type of stream piracy in western Virginia : university of Virginia Bulletin of the Philosophical Society, Scientific Section, v. 1, p. 437-442. Intercision refers to capture by the eroding of a narrow divide between 2 streams. Describes 3 examples of thi s in western Virginia, illustrated by topographic maps . In one case capture is ongoing via a subterranean passage .

Watts, w. A. , 1979, Late Quaternary vegetation of central Appalachia and the New Jersey Coastal Plain: Ecological Monographs , v. 59, p. 427- �69 . Describes late Quaternary vegetation in Appala-::hi"ns of Pennsylvania, west Vi rginia, and Virginia. Grass-dominated t\.mdra with dwarf shrubs was present 60 km south of the ice front at Longswamp, PA . Sedge tundra covered the higher mountains of central Appalachia . Climatically the periglacial region was cold, dry, and windy.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Weave r, C. E., 1978, Mn-Fe coatings on saprolite fracture surfaces : Journal of Sedimentary Petrology, v. 48, p. 595-610. Black coated fracture surfaces are common in saprolite. Many of the surfaces are polished and striated indicating movement has occurred . (Movement has been extremely gentle and is probably due to settling or stress release rather than tectonic activity. ) The surface skin of the black zone commonly consists of well oriented thin clay and biotite flakes coated wi th amorphous hydrous Mn-Fe oxides. Both the Mn and Fe were released from the biotite during acid weathering. Much of the Fe was precipitated in the vicinity of the biotite. The more mobile Mn migrated to pre-existing fractures and voids where the pH of ci rculating ground water was sufficiently high to cause precipitation.

Weave r, w. J., 1897, River adjustments in North Carolina : Elisha Mitchell Scientific Society Journal , v. 13, p. 13-24. OUtlines drainage evolution in parts of NC without benefit

of any maps or diag::ams•

•�ebb , D. K., Jr., and Collins , H. R. , 1967 , Geologic aspects of a recent landsline in Vinton County, Ohio: Ohio Journal of Science , v. 67 , p. 65- 74. Slide occurred along a highway in the abandoned valley 0f a minor tr�bu�ry of the Teays River system. A highly laminated lake deposit, similar in charactr.ristics to the Minford Silt, was the major component of the slide .

Webb , H. w., Nunan, w. E. , and Penley, H. M. , 1970, Road log - storm-damaged areas in central Virginia: Virginia Minerals, v. 16, p. 1-10. Road log to effects of damage due to Hurricane cami lle visible from roadways in selected areas of Nelson, Rockbridge , and Augusta counties.

Weems , R. E. , and Higgins, B. B., 1977, Post-Wisconsinan vertebrate remains from a fissure deposit near Ripplemead, Virginia: NSS Bul letin, v. 39, p. 106- 108. Fissures in a quarry wall nea� Ripplemead yielded fragmentary remains of at least 33 species of vertebrates. Most of the fauna is considered characteristic of post�isconsin time.

Welker, D. , 1982 , The ice age in We st Virginia: Mountain State Geology, 1982, p. 26-33. A popular outline of ice-age history of We st Virginia, including evolution of the Teays River system.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 We lls, S. G. , 1971 , Geomorphology of the sinkhole plain in the Pennyroyal Plateau of the Central Kentucky Karst [M. S. thesis]: Cincinnati , university of Cincinnati , 122 p. The history of succes�ive lowering of tl1e regional base level is preserved as a succession of cave levels and sinking streaws graded to the level of the caves. A new method using the equation of best fit curves permitted the projection of sinking streams' profiles from adjacent uplands beyond the streams ' terminal sinks to two levels beneath the present sinkhole plain surface. one level is coincident with the present ground-water level and the other coincides with a pre-existing higher level of ground-water recorded in a segment of a dry, abandoned , uppe r-level cave pascage . Two karst drainage basins in the sinkhole plain were delineated.

Wells, s. G. , 1976 , Sinkhole plain evolution in the Central Kentucky Karst: NSS Bulletin, v. 38 , p. 103-106. The geomorphic evolution of the sinkhole plain has involved successive lowering of regional base level �, d is indicated by two different cave levels. Subaerial portions of sinking streams can be mathematically extrapolated to these cave levels. Both subsurface arainage and thE regional slope of the Sinkhole Plain surface are concordant with th� di rection of max�mum groundwater slope and their ove rall patterns are not influenced by local structural and stratigraphic variation� .

Wentworth, C. K., 1923, The petrology and origin of the post-Miocene terrace gravels of the middle Atlantic slope [Ph.D. thesis] : Ames, Iowa, Io.ia State university, 302 p. Mainly a study of the Coastal Plaiu terraces, but also considen; Piedmont terraces and gravel deposits.

wentworth, C. K., 1928, Striated cobbles in southern states: Geological Society of America Bulletin, v. 39, p. ��i-954 . Striated cobbles have been found in the drainage basins of the Potomac , James , and Tennessee rivers drainage systems . Appea� ot to be present in modern stream gravels. Apparently they are ::;o not present in some of the older and higher terraces. The larger amount of striated clasts appear to have come from the headwater parts of the basins in which they occur . In some places, 25 to 33 percent of all larger cobbles show striations . Striations are considerably fainter than those on clasts from late Pleistocene drift. Suggests clasts were striated by action of thick river ice in jams during Pleistocene glacial climates.

Wentworth, C. K., 1930, sand and gravel resoutces of the Coastal Plain of Virginia: Vi rginia Geological Survey Bulletin, v. 32 , 146 p. Striated clasts and large boulders found in Virginia coastal Plain may indicate the action of ice jams and ice rafting during cold periods of the Pleistocene . The Sunderland formation is the highest terrace formation with such clasts. �- �triated clasts consist of dominantly hard, fine-grained quar• .te, and some dark-red quartzite and somewhat micaceous sanustonP. . Boulders 2 ft in diameter have been found not far from Chesapeake Bay. Large boulders and striated clasts are not found in modern sediments .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wentworth, c. K. , 1935, Striated rock surfaces in the St. francis River valley: American Journal of Science, v. 29, p. 364-368. Describes striated bedrock surfaces in stream channels, which Wentworth attributes to the action of river ice du ring Pleistocene cold periods.

Werner, E. , 1972, Development of solution features - Cloverlick Valley , Pocahontas County : We st Virginia Speleological Survey Bulletin, v. 2, 53 p. Caves appear to have been formed mainly by vadose and shallow phreatic water. Vertical position of cave passages is controlled by the local stratigraphy. Most caves are aligned along strike joints. surface topography has little effect on the alignment of cave passages. A probable subterranean stream pi racy is described.

We rner, E., 1972, Effect of small thrust faults on cave passage cross-section: NSS Bulletin, v. 34, p. 143-147. 'Ihrust faults with lengths of a few hundred meters and displacements in centimeters are common and exert contol over passage cross-section. Usually, the cave passage becomes slightly !:!SS in height and very much greater in w1dth where the faults intersect the passage . Gometimes the re is an accompanying increase in breakdown.

We rner, E. , 1973, Stratigraphic and structural control of cavern development in Pocahontas County, west Virginia, U.S.A. , in International Speleology: Proceedings of the Sixth International Congress of Speleology, p. 309-316 . cave passages have formed along the upper surfaces of ground water bodies perched on impermeable, insoluble, rock layers. vertical passages allow water from the land surface to fall to the level of ground water bodies, and horizontal passages allow drainage directly to the hillsides . Very simple ground water flow patterns are observed, probal:.ly due in part to the fact that no significant hydraulic head develop� underground .

We rner, E. , 1974, History and status of geological research in the west Virginia karst, in Rauch, H. w., and werner, E. , eds. , Fourth Conference on Karst Geology and Hydrogeology, 197 4, Proceedings : Morgantown, WV, wv Geological and Economic Survey, p. 1-9. Outlines history of geologic karst researcn, in tabular fonn. Map shows karst areas and exploration trends .

werner, E., 1974, Preliminary report on karst springs near Edray, northern Pocahontas County , west ·. nginia, in Rauch, H. W. , and werner, E., eds. , Fourth Conference en Karst �ology and Hydrology, 1974, Proceedings : Morgantown, wv, w.v. Geological and Economic Surv. , p. 25-28 . Seven springs along thE southern edge of Wolfpen Ridge were sampled over a period of time . 'Ihe degree of mixing appears to be related to flow rates; mere mixing occurs at the higher flow rates, as indicatoo by variabil ' ty between springs . Based on chemical parameters, all except one of the springs are conduit springs. 'Ihe water chemistry appears to be controlled by very local geology.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 werner, E., 1981 , Guidebook to the karst of the Central Appalachians , in Beck , s. F. , ed., Eighth Int�rnational Congress of Spelevlogy, Guidebook: Huntsville, AL, NSS , 51 p. Discusses major karst areas of the central Appalachians . Pages 1-30 are in English, p. 31-51 give German translation.

We rner, M. , and Moss, J. H. , 1969 , The large amount of colluvium in valley deposits near Lancaster, Pennsylvania: Pennsylvania Academy of Science Proceedings , v. 43, p. 183-184. Valley of Little Conestoga Creek is floored by a fill of sand and gravel size collJVium at least 14 ft thick . The colluvium is derived from the Antietam quartzite ridge , but extends 3/8 mi le downstream from the ridge . The colluvium is believed to have been deposited during a period of extreme periglacial frost action.

Wherry, E. P., 1923, The Blue Rocks of Greenwich Township: Historical Society of Berks County, Pennsylvania, Transactions, v. 3, p. 204-208 . Gives description of Blue Rocks boulder field.

White, C. H. , 1904, The Appalachian River versus a Te rtiary trans-Appalachian River in eastern Tennessee : Journal of Geology, v. 12, p. 34-39. Hayes and campbell coined the term "Appalachian River," and proposed that it drained through what is now the Coosa River to the Gulf until late Tertiary time , and was then captured by a tributary of the Susquatchie cutting through Walrlen Ridge. White argues against this theory and proposes an alternative . He says that up to the close of Cretaceous time, rivers flowed off toward the NW from the axis of the Great Smoky Mountains. After uplift of the Cretaceous peneplain, southwest-flowing subsequent streams formed in the Valley and Ridge . These have captured mst transverse-flowing streams with the exception of the Tennessee , which alone maintains its course across Walden Ridge . It is thus an antecedent stream.

WhHe, E. L., 1976, Role of carbonate rocks in modifying flood flow behavior : water Resources Bulletin (Urbana) , v. 12, p. 351-370. The interrelationships between the runoff characteristics of watersheds (expressed as the mean annual flood) , standard basin parameters (area, drainage properties, and relief), and the parameters which describe the solutional mdification of the basins (percent carbonate rock, sinkhole devel�pment , and measures of internal drainage ) were used to group and analyze 62 carbonate wa tersheds . The initial hypothesis was that carbonate rocks would have a dampening effect on runoff properties of drainage basins because of the rapid absorption of surface waters into the underground. Dampening does take place , but the influence of karst is no greater than the effects of other basin charact�ristics.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White, E. L. , 1977, Surface water hyd rology in carbonate basins within the Appalachians, in Tolson, J. s. , and Doyle, F. L. , eds., Karst Hycl rology: Memoir 12, International Association of Hydrogeologists: Internat . Asso. of Hydrogeologists, p. 377-389 . In order to maximize bett�en-group variance and minimize within-group variance the basins were divided into 3 homogeneous sets according to their peak flow flood behavior and into 2 homogeneous sets according to their l01rr-flow behavior. A refactoring of these resulted in two prediction equations for the mean annual flood for 2 of the basin subsets. The third subset , the most karstic, had no prediction equation because the relationships between runoff and the basin and karst properties break down when the basins are highly karstic. The basin subsets defined usina the sustained flow resulted in a subclassification separating conduit-flow from diffuse-flow basins.

White, E. L. , 1977, Sustained flow in small Appalachian watersheds ur.de rlain by carbonate rocks: Journal of Hydrology, v. 32, p. 71-86. Analysis of data from 57 carbonate basins shCNed that the basins fell into 2 distinct populations , those with sustained flows comparable to flows observed in non-carbonate basins and those with exceptionally low sustained flows . Basins with a high degree of karst development tended to have low su�tained flow because of poor groundwater storage and short residence times in carbonate aquifers with conduit-type permeability. Higher sustained flows were associated with aqui fers of the diffuse-flow type .

White, E. L., Aron, G. , and White, W. B. , 1986, The influence of urbanization on sinkhole development in central Pennsylvania: Environmental Geology and Wa ter Science , v. 8, p. 91-97 . Distinguishes "suffosioLlal" from solutional sinkholes. f'ormer are soil-piping sinkholes and constitute the principal landuse hazard of sinkholes. These sinkholes occur naturally but are exacerbated by runoff moditications that accompany urbanization. Suffosional sinkholes are typically 1.5-2.5 min diameter. The ve rtical transport of soil to foDD the void space and soil arch that are the precursors to sinkhole collapse is through solutionally widened fractures and cross joints. All aspects of soffosional sinkhole development nly commo take place within 10 m of the surface .

White, E. L. , and Reich, B. M. , 1970, Behavior of annual floods in limestone basins in Pennsylvania: Journal of Hydrology, v. 10, p. 193-198 . The mean of the annual series of floods, which corresponds to a flood with a recurrence interval of 2.33 years, is low in carbonate basins relative to that in clastic basins. The explanation proposed here is that stoDD excess water enters the growld water storage and then resurges slowly ove r the next few Jays . This results in lower floods for a given size of carbonate basin.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White, E. L. , and White , W. B., 1969 , Processes of cave rn breakdown: NSS Bulletin, v. 31 , p. 83-96. Some processes activating cavern breakdown are: 1) loss of buoyant support by draining of galleries; 2) undercutting of banks by floodwater stoping at the base level ; 3) removal of support by free surface stream action; 4) crystal wedging and attack by sulfate mineralization; 5) frost wedging; 6) unde rcutting by later cavern development; 7) undercutting and removal of material by vertical shafts and shaft drains; and 8) weakening of ceiling beds through attack by acid surface water. Breakdown takes place continuously and plays an important role both in the initial enlargement of the cavern system and in its final degradation.

White, E. L., and White, W. B., 1979, Quantitative morphology of landforms in carbonate rock basins in the Appalachian Highlands : Geological Society of America Bulletin, v. 90, p. 385-396 . Landfonn measures were devised for the drainage features and for dolines and applied to 62 small basins between Pennsylvania and Alabama. In addition to conventional drainage-basin measures, karst me�suree included carbonate rock fractions, measures of doline development, and measures of interr�l drainage . Various stream l.ength measures are related to the basin area in much the same way as streams in noncarbonate basins, showi�; the fluviokarst character of the Appalachian basins. The smallest and fewest dolines occur in the Ordovician dolomites and an intermediate size and numbe r in the Ordovician limestones. The largest and most nume rous dolines occur in £:at-lying Mississippian limestones. Factor analysis showed that the 15 measures used contained only 5 independent variables.

White, E. L. , and White, w. B. , 1983, Karst landforms and drainage basin

evolution in the Obey River ;.,_.. sin, north-central Ter;'!'lessee : Journal of Hydrology, v. 61, p. 69-82 . At the base of the CUmberland escarpment is an upland surface of doline karst developed in the Monteagle and St . Louis limestones at an elevation of 300-330 m. The internal drainage from the dolines and fran the sinking streams is perched on the impermeable Wa rsaw Formation and emerges as contact springs on the inner gorges of the rivers which have cut deep narrow valleys below the level of the upland surface . The longitudinal profiles of both active streams and underdrained channels were extrapolated through tlte doline karst. The active streams extrapolated emerge at grade with the present-day base-level streams . underdrained channels, hvwever, extrapolate to the upland surface and suggest that dry karst valleys can be interpreted much like river terraces. The development of interior drainage appears to be a much faster process than is the adjustment of the surface drainage .

Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White, E. L. , and White , W. B. , 1984, Flood hazards in karst terrains: Lessons from the Hur ricane Agnes storm, in Burger, A. , and Dubertret, L. , eds. , Hydrogeology of karstic te rrains: Case histories: Internat . Asso. of Hydrogeologists, p. 261-264. Frequently in the Appalachian karst the major streams remain on the surface while the tributaries are diverted to underground routes, with the water reappearing in the surface drainage through large limestone springs . Consider what happens to a flood pulse in this situation. Both sheetflow and runoff from nonkarstic tributaries are diverted into the subsurface through swallow holes. The net result is a damping of the flood pulse. This occurs because tt.a residence time of the water in the subsurface drainage system is longer than that of water in the stream. The flood hydrograph thus tends to have a lower peak and a somewhat more drawn out recession limb. An exceptionally high rainfall, however, overwhelms the subsurface drainage , and surface streams which are normally diverted to the underoround teturn to surface routes whether there is any surface channel or not .

White , w. A. , 1944, Determining factors in the coloration of granite soils in the southeastern Piedmont : American JrnJrnal of Science , v. 242, p. 361- 363 . Through its control of internal drainage , jointing also controls the alternati on of oxidizing and reducing conditions in the soil. Red soils develop on closely jointed granites because they have good internal drainage and oxidizing conditions prevail in them. Yellow soils develop on sparsely jointed granites because they ha·"e poor internal drainage and reducing condtions prevail in them �Jring a large share of the time.

White , w. A. , 1944, Geomorphic effects of indurated v.�neers on granites in the southeastern states: Journal of Geology, v. 52, p. 333-341. Indurated surficial veneers are a cha racteristic phenomenon on exposures of unjointed granite in the southeastern states. They are caused by deposition of iron oxides in the interstices between the partially dh;aggregated mineral ,.. '\ins of the "sap" rock at the

surface of the exposure . Brea��ing . · ��eers produces such peculiar erosional forms as weather p.. s, cavernous boulders, a"ld pedestal rocks.

�� ite, w. A. , 1945, Origin of granite dames in the southeastern Piedmont : Journal of Geology, v. 53, p. 276-282. The forms of the granite domes of the Southeast, which heretofore have been attributed to exfoliation, are regarded as the product of granular disintegration brought about by chemical weathering.

White , w. A. , 1950, Blue Ridge front - a fault scarp: Geological Society of America Bulletin, v. 61, p. 1309-1346. The present Blue Ridge scarp seems to have been produced by a late Te rtiary normal fault which runs nearly 700 mi les. Throughout much of its length, the fault seems to have utilized pre-existing structures of an older Triassic fault zone . The Ashevi lle peneplain of the upthrown block is considered correlative with the Piedmont peneplain on the downthrown block . Excellent sketches.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White, w. A •• 1952, Post-cretaceous faults in Virginia and North Carolina : Geological Society of America Bulletin, v. 63, p. 745-748. The idea that late def�rmation of the Appalachians has been accompanied wholly by gentle arching, tilting, or uplift, must be modified by the presence of normal and reverse faulting of post-Cretaceous age . Describes four such faults.

White, w. A., 1953, Systematic drainage changes in the Piedmont of North 561-580. Northeast-flowing tributaries of southeast-flowing rivers such as the Catawba , Yadkin, and James are long and subparallel . Opposing tributaries on the northeast sides of the main streams are short and irregular in direction. This asymmetry suggests the former existence of a subsequent drainage flowing northeastwa rd toward the Potomac. Apparently it was dismembered by multiple captures effected by short southeast-flowing streams of steeper gradient . Apparently, a succession of captures progressed across the area as the stronger southeast-flowing streams dismembered and diverted each of the NE-flowing streams in turn, beginning at the SE and ending at the foot of the Blue Ridge on the northwest. Elbows of capture are sharper in the NW streams where captures �re later. There, also, gravel-coated strath terraces are preserved across the divides between present major streams such as the Yadk in and catawba .

White, w. B. , 1960, Termina�ion of passages in Appalachian caves as evidence for a shallow phreatic origin: NSS Bul letin, v. 22 , p. 43-53. The dee� phreatic theory predicts cavern enlargement along any open conduit in a lithologically suitable bed without regard to depth below the water table. The shallow phreatic theory predicts solution only in a limited zone just below the water table . The latter theory was supported by evidence found in the examination of about 25 caves in the Appalachian Mountains. Caves with maze patterns have apparently fooned by slow ph reatic flow along a

soluble bed . In flat-lying limestones caves with this pattern may have considerable area, but in dipping strata, passages on the updip and downdip sides terminate abruptly. Hence solution is limited to a narrow horizontal zone even tho•Jgh the soluble bed continues in both directions .

White, w. B. , 1969, The Appalachian karst: An overview, in Fifth International Congress of Speleology, Stuttgart, 1969, Proceedings, Paper M-13, 5 p. Discusses characteristics of caves and karsts in the different physiographic provinces of the Appalachians .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White, W. B. , 1969, Conceptual models for carbonate aquifers : Ground Wa ter, v. 7, p. 15-21 . The very diverse types of ground-water behavior in carbonate terrains can be classified by relating the flow type to a particular hydrogeologic environment each exhibiting a cl"\aracteristic cave 100rphology. The ground water may IOOVe by diffuse flow, by retarded flow, or by free flow. Di ffuse flow occurs in less soluble rocks. Caves tend to be small and often little 100re than solutionally widened joints . Re tarded flows occur in artesian environments and where stratigraphy forces ground water to be confined tc relatively thin beds . Network cave patterns are characteristic. Solution occurs along many availabl e joints . Free flowing aqui fers are L, ose in which solution has developed a subsurface drainage system logically regarded as an underground extension of surface streams. Cave patterns typically are integrated co�Kruit systems .

White, W. B. , 1977, Conceptual mode ls for carbonate aquifers: Revisited, in Dilamarter , R. R. , and Csallany, s. c. , eds. , Hydrologic problems in karst regions : Bowling Green, KY, western Kentucky University, p. 1.76-187. A conceptual scheme for classifying carbonate aquifers in terms of groundwater flow system and hydrogeologic setting originally proposed in 1969 has been revised and extended to include factors of relief, r�ructure , and areal extent of the aquifer. Structural and topographic setting is shown to act mainly through determining the arrangement of karstic rocks with respect to sources of recharge and points of discharge . Lithologic and stratigraphic facto:s control the degree to which conduit permeability is developed. It is shown that a distinction between diffuse flow (fracture ) aquifer systems and conduit flow systems can be made in terms of their response to transient recharge events .

White, w. B., and Hess, J. w. , 1982 , GeoiOOrphology of � .ville Cove and the geology of the Butler Cave-Sinking Creek system: : ulletin, v. 44, p. 67-77 . The cove is an und�rdrained valley terminating downstream at a large closed depression. Fitting the valley profile to exponential functions permits correlation of valley levels with terrace levels in the Bullpasture River. The Butler Cave-Sinking Creek system has an ove rall pattern of a network maze with orientations controlled by the local joint pattern. The cave contains a complex boulder and cobble fill that seems to represent a rapid infilling event of pre-Wi sconsin age .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 White , W. B., Scheetz . B. E. , Atkinson, S. D. , Ibberson, D. , and Chess, C. A. , 1985, Mineralogy of Rohrer's Cave , Lancaster County, Pennsylvania : NSS Bulletin, v. 47, p. 17-27 . The cave contains a bizarre collection of white and black soft mushy coatings and hanging forms resembling pinecones . It also contains brown stalactites and stala�·ri tes of hyd rated iron oxides. The black coatings consist of manganese oxides with exceptional concentrations of the heavy metals nickel, cobalt, copper, and zinc . The white opaline or moonmi lk-like deposits consist in part of noncrystalline hydrated allumUnum silicates and aluminum phos�rates. Their chemical composition and microstructual identify them as the clay mineral allophane .

White, w. B., and Schmidt, v. A. , 1966, Hydrology of a karst area in east central West Virginia: Wa ter Resources Research, v. 2, p. 549-560 . The water table is remarkably flat, with abrupt breaks in slope only near the margins of the area unde r a rugged surface topography whose relief exceeds 2000 ft. The surface topography is not reflected in the karst water table, and free-surface flow often occurs as much as 1000 ft below the land surface . Even minor insoluble beds are capable of perching tributary underground streams as much as severdl hundred ft above base level. underground flow takes piace along hydraulic gradients that point to the major base-leveling stream of the area, the Greenbrier River, rather than to surface valleys .

White, w. B., Watson , R. A. , Pohl , E. R. , and Brucker, R., 1970, The Central Kentucky Karst: Geographical Review, v. 55, p. 88-115. An informative, well-illustrated review of landscape evolution in the Central Kentucky Karst.

White , w. B., and White, E. L. , 1974, Base-level control of unde rground drainage in the Potomac River basin, in Rauch , H. w. , and Werner, E., eds., Fourth Conference on KarEt Geologf and Hydrology, ProceediP.gs : Morgantown, WV, w. v. Geol . and Econ . Survey, p. 41-53. Davies' premise that cave levels correlate closely with river terraces, and therefore records periods vf quiescence in valley downcutting, was re-examine� using recently available data on the cave elevation distributions for the entire Potomac River basin. Bar diagrams of both cave-length arn cave-entrance distributions show pronounced maxima that correlate with river profiles. Best correlations exist in the downstream reaches where the e"osion surfaces are best developed. Cave-level profiles parallel river profiles and suggest that river slopes have been invariant for considerable periods of time .

White, w. B., and White, E. L. , 1983, Patterns of cave development and speleogenesis in West Virginia, in Medville, D. M. , Dasher, G. R. , and Werner, E. , eds ., An introduction to the caves of east-central West Virginia: Guidebook for the 1983 NSS Convention (NSS Convention Guidebook 23): Huntsville, AL, NSS , p. 7-24. A general dis�ussion of factors affecting cave development in We st Vi rginia.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Whi tehead , D. R. , and Barghoorn, E. S., 1962, Pollen analytical investigations of Pleistocene deposits from western North Carolina and South Ca rolin�: Ecological Mon�graphs , v. 32, p. 347-369 . Conclude that organic horizons , ovP. rlain by up to several tens of feet of colluvium, were probably deposited du ring a Pleistoc�ne interstadial greater than 35,000 yr BP. They represent organic sediment that acCUimllated in shallow boggy basins perhaps daimned by mass-wasting associated with a glacial age . Two periods of colluviation separated by a period of soil development have been responsible for the burial of the organic horizons . There is some evidence that the climate at the beginning of the period of deposition was cooler and that it underwent a gradual amelioration as the interval progressed. Gives 4 radiocarbon dates from 2 sites, 1 greater than 30, 000 yr a� the other 3 greater than 35,000 yr.

Whitley, L. D. , 1977, Karst topography and its occurrence in Kentucky, in Dilamarter, R. R. , ed ., Hydrologic problems in karst regions : Bowl ing Green, KY, Western Kentucky University Press, p. 41-49 . A very general dis�JSS1on of karst processes and occurrence of karst landforms in Kentucky.

Wh itney, J. A. , Jones, L. M. , and Walker, R. L., 1976 , Age ana origin of the Stone Mountain Granite , Lithonia district, Georgia: Geological Society of America Bulletin, v. 87 , p. 1067-1077 . Jepth of intrusion suggested for the Stone Mountain pluton requires that 10-15 km of material has been reJOOVed since Late Penn sylvanian time . Even considering l.he thickness of unmetamorphosed Paleozoic section to the north, however, there is little evidence to suggest mere �� 6-8 km of erosion during this period. WhatP.ver the details of the tectonic process, it appears that the inner Piedmont now exposed east of Atlanta has unde rgone large amounts of uplift subsequent to Late Pennsylvanian time.

Whi ttaker, R. H. , 1956, Vegetation of the Great Smoky Mountains: Ecological Monographs , v. 26 , p. 1-80 . Discusses distribution of tree species as a function of moisture and elevation. Describes 15 vegetation types (e.g., Cove ha rdwoods forest ).

Whittecar, G. R. , 1984, Late Quaternary deposits in small valleys , western North Carolina Piedmont [Abstract ): Virginia Journal of Science , v. 35, p. 125.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Whittecar, G. R. , 1985, Stratigraphy and soil development in upland alluvium and colluvium, north-central Virginia Piedmont: Southeastern Geology, v. 26, p. 117-129. One-meter thick colluvium blanketed the landscape except where ove rthickened along active and relict toeslopes. Alluvium lies in channels along erosional benches. Bedrock is present only under valley bottoms along large •reams . Colluvium truncates saprolite st ructures sharply, only rarely showing upwa rd sequences of progressively greater amounts of movement due to soil creep. Va rying amounts of weathering and soil formation denoted multiple ages of colluvium and alluvium along selected reaches of the ditch; soil colors and percent clay in the B horizon proved most useful in establishing relative ages of deposits. Epi sodic colluviation was apparent at several locations. Several lines of evidence suggest that only a few tens of meters of relief formed during Pleistocene .

Whittecar, G. R. , 1988, Colluvium and alluvium in terraces and debris-filled hollows, western North Carolina Piedmont [Abstract): Geological Society of America Abstracts with Programs, v. 20 , p. 322-323. Up to 6 m thick, the colluvium is usually massive but can contain subhorizontal iron pan concretions 1 em thick and lenses of laminated silt and clay. Dissected and indistinct terrace remnants contain the most deeply weathered colluvium. Bt horizons ( 5YR to 7 .5YR) , formed in this colluvium but truncated by modern slopes, exceed 1 m in thickness. Wood fromcolluvium-bu ried alluvium beneath one terrace was dated at greater than 40,000 yr B.P. (w-5114 ). Colluvium that partially fills first-order valley swale� is less weathered. Relatively rapid slope processes induced by harsh glacial-·age climates probably are responsible for the colluvium observed. The oldest colluvium may predate the last interglacial (Stage 5).

Williams, G. P. , and Guy, H. P., 1971 , Debris avalanches - a geomorphic hazard, in Coates, D. R. , ed., Environmental Geomorphology: Binghamton, NY, S.U.N. Y. PUblica. in Geomorphology, p. 25-46 . Presents measurements and a description of the avalanche scars 30d analyzes the possible factors associated with the occurren�e of these debris-avalanches produced in Virginia by Hurricane Camille in 1969 . The presence of pre-existing depressions on the hillside and the aspect of hillside (N-, NE- , and E-facing slopes ) were associated with the most intense avalanching. Most debris avalanches occur during the sUIIIIlertime. Much but not all of the damage resu. ting from debris avalanches can be prevented by careful planning.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Williams, G. P. , and QJy , H. P. , 1973, Erosional and depositional aspects of Hurricane camille in Virginia, 1969: U.S. Geological Survey Professional Paper, v. 804, BO p. Describes the consequences of about 28 inches of rain falling on central Virginia in about 8 hours on the night of August 19-20 , 1969 . Erosion resulted mainly from debris avalanches down the mountain sides and channel scour along streams. Tctal amount of sediment yield from certain a.�as was the equivalent of several thousand years of normal erosion . Discusses morphology and occurrence of these avalanches. 'I1'le types of sedi!IIE•nt deposits were 1) debris avalanche at the base of hillslopes (rare); 2) mountain-stream channel deposits; 3) alluvial fans; .4 ) delta-like deposits at the junction of a stream and major highway; 5) accretion deposits on flood plains.

Williams, K. F. , and Rec.J, L. A. , 1972, Appraisal of stre&n sedimentation in the Susquehanna River basin: u.s. Geological Survey Water--Supply Paper, v. 1532-F, p. Fl-F24. Table 2 shows sediment yields for 42 sub-basins. Fig. 3 shows generalized averages. Geology in the Valley and Ridge appears to be a variable that affects sediment yields, because ba��ins with more than 25% limestone have significantly lower sediment yields than basins with identical land use but no carbonates . Piedmont streams have significant suspended-sediment concentrations most of the time, whe reas other streams have t.his only during and for a few days after storms . The average particle size of sediment is the same for all physiographic provinces.

Willis, B., 1887, Topography and structure in the Bays Mountains , Tennessee : School of Mines Quarterly, v. 8, p. 242-252. The Bays Mountains are the product of structure , rock resistance , and position of base level ; the first two are given, the last is constantly sinking.

Willis, B., 1889, Round about Asheville: National Geographic Magazine, v. I, p. 291-300. Outlines landscape evolution of area: 1) Appalachians base-levelled; the balds of the unakas represent the heights of that first-known erosion surface ; 2) topography of the area revived by an upl ift of 3,000 ft or more, div!.ded by 2 intervals of rest; during the first, the Asheville base level was formed; during the second, the valley alone was reduced; 3) the latest movement of the uplift has been quite recent and the streams have accomplished but a small part of their new task .

Willis, B., 1895, The Northern Appalachians : National Geographic Society Monograph, v. 1, p. 169-202 . Describes physiography and discusses landscape and drainage evolution.

Wilshusen, J. P., 1979, Geologic hazards in Pennsylvania: Pennsylvania Topographic and Geologic S•:rvey Educational Series, v. 9, 56 p. A popular account of geologic hazards, particularly various

forms of mass movement and subsidence (sinkholes) •

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wilson, J. R. , 1977, Lineaments and the origin of caves in the Cumberland Plateau of Alabama: NSS Bulletin, v. 39, p. 9-12. Location of springs and caves along lineaments is attributable to the greater solution along the zones of fracturing. '!his is particularly true at lineament intersections . Simple caves may form anywhe re as a result of normal jointing and rock solubility. In areas of moderate to high relief, a) deep simple caves form along lineaments and b) complex caves form at the intersection of lineaments .

wilson, J. T. , and Fairbridge , R. w. , 1971, Appalachian peneplains, paleosols, and plate tectonics [Abstract ): EOS (American Geophysicatl union Transaction), v. 52, p. 350. 'lbree major cycles of peneplanation in the Appalachians came to an end respectively about 200, 130, and 60 million Y£!ars ago - Pre-Newark, Fall zone , and Schooley. Each erosion surfc1ce is designated by specific features and paleosols. Repeated uplift of these peneplains can hardly be explained by revivals of Appalachian roots or by isostatic response to unloading, neither of which should have a 60-million year scale or greater. on the other hand, the cyclicity shows some similarily to major episodes of plate tectonics , and uplift could be a response to high heat-flow epochs .

Wilson, R. L., 1984, Slump features at Montlake in southeastern Tennessee previously misinterpreted as a sinkhole [Absttact): Gt::,,logical Society of America Abstracts with Programs, v. 16 . �· 206. Montlake lies atop the Cumberland Plateau 330 m from the edge of the escarpment. Previously it has been interpreted as a sinkhole formed by the collapse of underlying strata into a giant cavern. Mapping and satellite images, however, suggest that it was formed by down-.lope move�DP.nt of la:-ge masses of Sewanee Conglomerate along a series of intersecting joints.

Wilson, W. F., carpenter, P. A. , III, and Conrad, S. G. , 1976, North Carolina geology and mineral resources : A foundation for progress: N�rth C&rolina Division of Resource Planning and Evaluation, Mineral Resources Section, Educational Series, v. 4, 78 p. A popular account of geology of NOrth carolina. Has short section on physiography, together with a physiographic map. Provides a brief summary of bedrock geology.

Winker, c. D. , and Howard, J. D. , 1977, Correlation of tec1:onically defonne.� shorelines on the southern Atlantic Coastal Plain: Gel)logy, v. 5, p. 123- 129 . Topographic shoreline features were mapped and differentiated into age groups on the bases of progradational discontinuities, contrasts in state of preservation, and changes in coastal morphology. 'lbree shoreline sequences are well preserved ,

permitting paleogeographic reconstructions . A combination e published and di rect geomorphic evidence suggests that all three shoreline sequences have been deformed.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wol fe , P. E. , 1943, Soil and subsequent topography: Jou rnal o� Geology, v. 51 , p. 204-211. Fluvial erosion acting on a series of plunging synclines and anticlines has etched out a subsequent topography the details of which correspond intimately with structural , lithologic, and soil variations . A fine-textured erosional pattern on the dip slopes as contrasted with a coarse-textured pattern on the scarp slopes of the strike valleys is explained on the basis of soil-erosibility c�ifferences. The synclinal interfluves developed on the smaller f�lds within the major syncline have a distinctive topography which consists of 4-10 ft strike ridges and valleys spaced 50-100 ft apar·+:, termed a "strike-vale-and-ridge" topography .

WOl fe , P. E. , 1953, Periglac1al freeze-thaw basins in New Jersey: Journal of Geology, v. 61, p. 131-141 . The b�sins are oval , irregular, shallow depressions , without rims or orientation, and occur on all lithologic formations . The presence of extensive frost-wedge fillings, involutions , festoons , and other frost structures indicate that the area was exposed to a colder climate than that of today. The origin of the basins is attributed to frost-thaw action .

WOlfe, P. E. , 1977, The geul�- and landscapes of New Jersey: New York, Crane , Russak & Co. Discusses geomorphology and glacial geology of New Jersey on pages 188-275.

Wolfe , T. E. , 1964, cavern deve!opment in the Greenbrier Series, West Virginia: NSS Bulletin, v. 26, p. 37-€0. The conclusions drawn with the aid of cross sections �.ndicate that a major etosion level , described �s the Harrisburg peneplain, appears to have been a key factor in the local development of major horizontal cave passages. Their accordance may have been produced as a result cf water table stabilization ove r a long period during the planation of the erosion level .

Wolfe , T. E., 1973, Sedimentation in karst drainage basins along the Allegheny escarpment in southeastern West Virgi�ia, U.S.A. [Ph.D. thesis): Hamdlton, Ontario, McMaster University, 446 p. By examining streams, surface s��imentation, and cave fills within the basin, the author attempts to show that a relationship between surface and subsurface deposits exists. Through the use of traceable identifiers such as quartz pebbles derived from the Princeton and Pottsville formations, a hypothesis of stream reversal and subterranean piracy was supported. Scallops indicate velocities of different magnitude and direction from those responsible for bedload transport, indicating deposits were laid down sometime after passage formation. Some caves show evidence of massive, single-deposition events, suggestive of periglacial events.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wol fe , T. E. , 1975, Karst sieve deposits, in Panos, V. , ed., Sixth International Congress of Speleology, Proceedings : Prague , Academia, p. 557-565. Where streams flow from higher elevations of noncarbonate rock onto low-lying carbonate terrain, alluvial material is often deposited in a fan-shaped for !. Auth�r considers such deposits the result of surface drairagA being diverted underground upon reaching a highly karstified surfac.• , so that stream competPnce and capacity drop rapidly. Sue�. diversion usually occurs at several places along the channel. Sh•ve deposits result from the deposition of surface stream �l load when surface drainage is filtered through the alluvial veneer of the !;urface streams to undergroUI'l!! conduits. They occur. frequently along the clastic/carbonate bedrock contact . It seems probable that the greatest source for these deposits was derived from periglacial mass movement .

Wolman , M. G. , 1955, The natural channel of Brandywine Creek , Pennsylvania: u.s. Geological Survey Professional Paper, v. 271, 56 p. When casually obse�·ed, the channel of Brandywine Creek is a picture of disorder. To the ntrary, co however, measurements of discharge , width, depth, velocity, slope , suspended-sediment load, and the computation of a roughness factor indicate that the cross-sectional form and the gradient cf the channel actually approach a dynamic equilibrium.

Wolman , M. G., 1967, A cycle of sedimentation and erosion in urban river channels: Geografiska Annaler, v. 49A, p. 385-395 . Historical evidence and contemporary measurements indicate that successive changes in land use have been accompanied by changes in sediment yield and in the behavior of stream channels. Serlimer.t yields in pre-farming times appear to have been less than 100 tons;sq . mi.;yr . Yield� from agricultural lands range from '300 to 800. Areas exposed during construction can produce sediment loads in excess of 100,000 . Increased runoff from urban areas coupled with a decline in sediment yields to values of 50-100 promote bank erosion and channel widening.

Wolman , M. G. , and Leopold, L. B., 1957 , River flood plains: Some observations on their formation: u.s. Geological Survey Professional Paper, v. 282-c, p. 86-109. Proportion of ove rbank deposits generally small relative to channel deposits. It i� difficult to differentiate between the two in a stratigraphic sect.�n alone , however. The flood plains of many streams are subject to flooding about once a year. Contains data on Piedmont streams.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wolman , M. G., and Schick, A. P. , 1967 , Effects of construction on fluvial sediment, urban and suburban areas of Maryland: Water Resources Research, v. 3, p. 451-464 . Sediment concentrations from areas undergoing construction range from 3000 to over 150, 000 ppm, whereas in natural or ag•icultural catchments the highest is 2000 ppm. Yields from construction areas range from several thousa..,j to a maxiiiDJIII of 140,000 t/square kilometers/yr . Sediment storage occurs on construction sites as well as in valley bottomlands . Roadcuts show similar sediment yields. Imposition of large quantities of sediment on streams previously cartying relatively small quantities of primarily suspended material produced dramatic changes.

Wood , B. R., 1969, Ge0100rphology of Eblen cave-oouth deposits and associated karst phenomena [M.S. thesis] : Knoxville, TN, University of Tennessee, 121 p. Cave-oouth deposit is the result of three periods of depo sition: 1) large angular blocks of breakdown, probably result of periglacial frost action; 2) sediments resulting from Indian habitation; 3) deposits by Civil War saltpeter miners.

Woodruff, J. F., 1964, A comparative ar4lysis of selected drainage basins : Profe:;sional Geographe r, v. 16, p. 15-19. Provides data on bifurcation ratios , drainage densities, etc., for some areas in Valley and Ridge , among others.

Wood ruff, J. F., 1964, A morphometr�c analysis of so• .va Piedmont sub-regions : Southeastern Geographer, v. 3, p. 17-24 . Attempts to provide a quantitative basis for the Washington Plateau, Midland Slope , and Atlanta Plateau subregions . Used stream lengths, drainage basin areas, drainage density, and hypsometric cur-res to do so .

Woodruff, J. F., 1964, The Piedmont peneplain: American Geographers Southeastern Division Memorandum Folio, v. 16, p. 121-130. Statistical and graphical analysis of the elevation of crests on the Piedmont would seem to verify the presence of an old upper surface of erosion. There is a significant grouping of higher crest elevations, but there is no distinct accordant upper surface even vaguely resembling that surface so often diagrammed in basic texts as being the rejuvenated peneplain.

Wood ruff, J. F •. 1971, Debris avalanches as an erosional agent in the Appalachian Mountains: Journal of Geography, v. 70, p. 399-406 . Describes characteristics of debris avalanches in central Virginia resulting from Hurricane camille. Suggests debris avalanches are responsible for formation of drainage patterns, as foll0WS . Prior to the storm, ground water moved along preexisting fractures, resulting in thicker soils above the fractures. Because of these thicker soils, such location:. are the sites that fail and become debris avalanches. A trough is thus formed, which becomes the focus of future drainage .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Woodruff, J. F. , and Parizek , E. J., 1956, Influences of underlying rock structure on �tream courses and valley profiles in the Georgia Piedmont: Association of American Geographers Annals, v. 46, p. 129-139 . Longitudinal gradients of major streams were plotted and related to geology. In general , high points on the profiles and the resulting shoals occur where resistant migmatite and monzonite have pierced the widespread "carolina rocks." Where rivers shoal at nick points the valley is youthful, while upstr

Woods, E. B. , 1974, Spatial variation of hillslope profiles in the Cumberland Plateau, Kentucky: Professional Geographer, v. 26 , p. 416-420. Measured hillslo� profiles on Breathitt Formation (interbedded sandstones, siltstones, and a few coal beds ). 77% of slope profiles were either convex ove r concave (43.6%) or convex 133.8\i. The profiles tend toward being in the mature stage in the Davisian sense.

Woodson, F. J. , 1981, Lithologic and structural controls on karst landforms of the Mitchell Plain, Indiana , and Pennyroyal Plateau, Kentucky [M.S. thesis]: Terre Haute, IN, Indiana State university, 132 p. Discusses differences in sinkhole morphology on different stratigraphic units, distinguishing Ste. Geneviev�- and St. Louis-type sinkholes. Although the origin and persistence of geomorphic outliers is related to lithology, their distribution is governed regionally by the declination of strata and locally by pre-Pleistocene drainage patterns. Also discusses historical geomorphology.

WOOdward, H. P., 1936, Natural Bridge and Natural Tunnel , Vi rginia: Journal of Geology, v. 44, p. 6�4-616 . Suggests Natural Bridge and Natural Tunnel had similar origins; they are both the remnants of underground passages that were formed when surface streams were diverted underground. Illustrated with landscape sketches.

Woodworth, J. B., 1894, The relation between baseleveling and organic evolution: American Geologist, v. 14, p. 209-235. Puts forth some rather archaic hypotheses, for example that since pe�eplains are flat they must have large amounts of swamps , so that the existence of a peneplain in Jurassic-cretaceous times helps explain why reptiles were dominant then.

Wrigr.t , F. B., 1896, The origin of the Wind Gap: American Geologist, v. 18, p. 120-123. The ge�eral appearance of the notch is such that one cannot help believing that at some time a stream ran over Blue Mountain at this point and cut the gap. Waterworn pebbles found in excavation. Suggests this stream was captured by Lehigh or Delaware river.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 wright , F. J., 1925, The physiography of the uppe r James River basin: Virginia Geologica' Survey Bulletin, v. 11 , 67 p. Discusses physiography using the �rosion-cycle frame of reference . Also discusses rock-cut terraces, which show little uniformity in terrace levels and therefore probably do not correlate with cycles or partial cyclas of erosion.

Wright , F. J., 1927, The Blue Ridge of sc•1thern Virginia and western North Caroli�: Denison University Bulletin, Journal of the Sci . Lab. , v. 22 , p. llS-132. Discusses possible origins of the Blue Ridge escarpment , including theories of fault scarp, warping, marine sea cliff, peneplains of different ages, peneplains of same age , superior rock resistance .

Wright , F. J., 1927, Gravels on the Blue Ridge : Denison University Bulletin, Jourr�l of the Scientific Laboratories, v. 22, p. 133-135. Suggests rounded gravels on the Blue Ridge may be Cretaceous in age , lying on a remnant of a peneplain of that age .

Wright, F. J., 1928 , The erosional history of the Blue Ridge : Denison University Bulletin, Journal of the Scientific Laboratories, v. 23 , p. 321-344. Suggests upland peneplain along Blue Ridge summit is older than the Piedmont peneplain.

wright, F. J. , 1929, Stream piracy near Asheville, North Carolina: Denison University Bulletin, Journal of the Scientific Laboratories, v. 24, p. 401-406. Presents evidence that Hominy Creek , a tributary of the French Broad, has pirated tributaries of the Pigeon River.

Wright, F. J., 1931, The Older Appalachians of the South : Deni son University Bulletin, Journal of the Scientific Laboratories, v. 26 , p. 143-250 . Discusses erosion cycles and correlation of peneplains , the origin of the Blue Ridge scarp, and selected problems in drainage evolution .

wright , F. J., 1934, The New Appalachians of the South : Part I. Between the Potomac and New rivers: Denis.:>n University Bul letin, Journal of the Scientific Laboratories, v. 29, p. 1-105. Erosion during the Har risburg cycle was especially important in the development of the present topographic features of the region. During this cycle, the Harrisburg peneplain cond mmerous local peneplains and mature valleys in the Appalachian Ridges were produced. These features are tentatively correlated with the Piedmont peneplain. Also discusses drainage evolution, karst eeatrues, and Natural Bridge .

Wright , F. J., 1936, The Natural Bridge of Virginia: Virginia Geological Survey Bulletin, v. 46-G, p, 51-78 . Similar to discussion in 1934 pape r.

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Wright , F. J., 1936, 'nle Newer Appalc.. , of the �"outh: Part r:.:. South of tile New River: Denison university �ul letin, Journal of the Scientific Laboratories, v. 31, p. 93-l42 . Discusses region in framework of erosion cycles. Also notes that terraces are not at unifonn elevations above the present valley floors . 'nley are, furthennore, very irregular in the ext�nt of their development, and also iUj te variable in number even in different parts of the same val".ey. Also discusses Burke Garden, Natural TUnnel , sinkholes, and supe r�osed drainage .

Wright, F. J., 1942, Erosional history cof tr.e Southern Appala·::hia·1s: Journal of Geomorphology, v. 5, p. 151-161 . Gives SUIIIIIary account of erosior: cycles in the southern Appalachians and their significance for landscape evolutio�.

Wright, H. E., Jr., Spross, B. , and Watson, R. A. , 1966, Pollen analyses of the sediment from sinkhole ponds in the Central Kentucky �rst: NSS Bulletin, v. 28, p. 185-189 . Fran cores in sinkhole sediments, �uthor found a h '.c;" percentage of ragweed pollen and thvs concluded that most of the f1:.. ... i.; moae rn. Provides evidence that sinkholes are actively formdng and are subject to rapid sedimentation. Indicates sinkholes are likely to be poor locations for long pollen records (since proven untrue ).

Wright, R. J., 1942, underfit meanders on the Frer.ch Broad River, North Carolina: Journal of Geomorphology, v. 5, p. 183-190 . Explains unnerfit meanders a� the result of 1) loss in volume due to increasing underflow through alluvium; 2) reduction in discharge through piracy in the present cycle ; and 3) the contrast between large entrenched meanders and smaller floodplain meanders. !t. seems unlikely that climatic change has been a contributinq factor.

Wyrick , G. G., and Borchers, J. w. , 1981, Hydrologic effects of stress-relief fracturing in an Appalachian valley: u.s. Geological Survey water-supply Paper, v. 2177, 51 p. A hydrologic study wasmade to determi•� how stress-re!ief fracturing affects the occurrence and movement o! ground water in a typical Appalachian ..alley. 'nlese systems constitute the most transmissive part of the regional aquifer and affect surface-water hydrology in the area. Ground water occurs mainly in horizontal bedding-plane fractures under the valley floor and in nearly vertical and horizonlal �lump fractures along the valley wall.

Yo rk , J. E. , and Oliver, J. E. , 1976 , Cret�ceous and Cenozoic faulting in eastern North America : Geological Society of ."o0111::ric:; Bulletin, v. 87, p. 1105-1114. Table 1 lists known faults in eastern North America, together with type of fault, displacement , and youngest faulted rocks .

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Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3744468/9780813759197_backmatter.pdf by guest on 27 September 2021 Zisa, A. C. , 1976, A geomorphic inve stigation of the Wadesboro Triassic basin [M.A. thesis] : Athens, GA, University of Georgia, 84 p. Performed morphometric analyses of drainage basins in Wadesboro ba�in and flanking Carolina slate belt and Sandhi lls in order to see how they differed. Found few differences, indicating that the geological distinctiveness of the Wade sboro basin does not carry over to geomorphic distinctiveness .

Zurawski, A. , 1977, Summary appraisals of the nation's ground-water resources Te�•essee region : U.S. Geological Survey Professional Paper, v. 813-L , 35 p. Discussion of occurrence of ground water in the different physiographic provinces shows relation between bedrock and su rficial geology and groundwater storage;mvvement .

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