EGSP SERIES N0.I3 
 
 L. 
 
 3 0112 061546245 
 
 MORGANTOWN ENERGY TECHNOLOGY CENTER 
 
 
 BLACK SHALE AND SANDSTONE FACIES OF THE DEVONIAN 
 "CATSKILL" CLASTIC WEDGE IN THE SUBSURFACE 
 OF WESTERN PENNSYLVANIA 
 
 / 
 
 K) 
 
 By R.G. Piotrowski and J.A. Harper 
 
 a 
 
 Prepared by 
 
 PENNSYLVANIA DEPARTMENT OF ENVIRONMENTAL RESOURCES 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC SURVEY 
 Contract Number EY-76-S-05-5I98 
 
 UNITED STATES 
 DEPARTMENT OF ENERGY 
 
 PREPARED UNDER CONTRACT TO THE 
 EASTERN GAS SHALES PROJECT 
 (EGSP), 1979 
 
 UNIVERSITY OF ILLIN0I# 
 GEOLOGY LIBRARY 
 
BLACK SHALE AND SANDSTONE FACIES OF THE DEVONIAN "CATSKILL" CLASTIC WEDGE 
 
 IN THE SUBSURFACE OF WESTERN PENNSYLVANIA 
 
 by 
 
 Robert G. Piotrowski 
 John A. Harper 
 
 First printing 1979 
 Second printing 1980 
 

 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
BLACK SHALE AND SANDSTONE FACIES OF THE DEVONIAN "CATSKILL" 
 
 CLASTIC WEDGE IN THE SUBSURFACE OF WESTERN PENNSYLVANIA 
 
 INTRODUCTION 
 
 Black organic-rich shales are common constituents of sedimentary sequences 
 deposited throughout geologic time in many areas of the world. Twenty-six states 
 in the United States and six Canadian provinces and territories are underlain by 
 sedimentary rocks containing Devonian and Mississippian black shales (Provo, 1976). 
 In the eastern United States, Devonian black shales are found in the Appalachian, 
 Illinois, and Michigan basins. Natural gas has been produced from these shales 
 for over 150 years. 
 
 Historical Review 
 
 The first well in the United States drilled specifically for natural gas had 
 gas production from Devonian black shales in 1821, 38 years prior to the drilling 
 of the historical Drake oil well. This shale gas well was drilled in Fredonia, 
 Chautauqua County, New York, and produced enough gas to provide street lighting 
 for the town. With that discovery, drilling commenced along the south shore of 
 Lake Erie from Dunkirk, Chautauqua County, New York, to Sandusky, Erie County, 
 
 Ohio. The gas produced from the shales was a valuable commodity available at 
 shallow depths. The low pressure wells had relatively small open flow rates but 
 long life spans. Drilling in the area continued throughout the 1800’s and into 
 the early 1900's, but the discovery of high flow rates from Upper Devonian sand¬ 
 stone reservoirs quickly put a damper on shale gas activity. There is very little 
 information on these early shale gas wells other than some descriptive data. 
 
 In Pennsylvania, the Lake Erie shale gas trend is represented by three fields. 
 North East, Erie, and Girard (Figure 1). These fields were discovered between 
 1860 and 1880, and although initial production from the discovery wells was 
 small, the fields are still productive. Ashley and Robinson (1922) reported 
 that the wells in these fields were drilled to an average depth of 1000 feet. 
 
- 2 - 
 
 and had highly variable rock pressures and gas volumes. They also noted that the 
 North East field produced small quantities of oil as well as gas. Some gas was 
 usually encountered during water well drilling. In 1928, Frank Warner of Cranes- 
 ville, Erie County, drilled a water well on his property to a depth of 36 feet 
 and encountered enough gas for domestic use. 
 
 Some data are also available for 20 wells drilled in the Girard field in 
 1941 by the Ohio Oil Company (now Marathon Oil Company). These wells, located 
 in Springfield Township, Erie County, Pennsylvania, and Conneaut Township, 
 Ashtabula County, Ohio, had open flow rates ranging from a low of 116,000 cubic 
 feet of gas per day to a high of 4,168,000 cubic feet of gas per day. None of 
 the wells produced from a depth greater than 800 feet. Between 1941 and 1961 
 drilling for shale gas was virtually at a standstill in Pennsylvania. Only two 
 wells are known to have discovered gas in the Upper Devonian shale in the 1960's. 
 The Carter #1 well in Conneaut Township, Crawford County (Figure 1) was originally 
 drilled as a test of the Medina Group (Lower Silurian) and completed as dry in 
 that zone in June, 1961. It was plugged back to 400 feet so the farmer could 
 use the gas encountered in the shale. Leon Matezak drilled a well on his property 
 in 1964 that produced gas from a 350 foot thick zone in the shale. The open flow 
 was gauged at 15,000 cubic feet per day with a rock pressure of 22 pounds. 
 
 Recent Shale Gas Activity 
 
 With the onset of energy shortages and the subsequent increase in natural 
 gas prices, interest has been renewed in the Devonian shales and their potential 
 natural gas resources. Since 1975, 11 wells have been reported in Pennsylvania 
 that produced or had the potential to produce from black organic-rich Devonian 
 shale (Figure 1). The first such well, the Metropolitan Industry #1, in 
 Darlington Township, Beaver County, was originally drilled as a test of the 
 Medina Group (Lower Silurian) by Quaker State Oil Refining Corporation. No 
 gas was encountered in the Medina, and the well was plugged back to 4,550 feet 
 
Figure 1. Locations of significant shale-gas wells and fields in Pennsylvania 
 
- 4 - 
 
 to test the Devonian Rhinestreet shale facies. There was no natural production 
 from the shale, but after hydraulic fracturing the well initially produced 
 150,000 cubic feet of gas per day with a rock pressure of 1150 pounds. This 
 flow did not last long, however, as the gas blew down after only 30 days of 
 production. When it was shut in, the well would again build up pressure, but 
 when opened it would quickly blow down to nothing. Piotrowski (1978) postulated 
 that there was little natural porosity in the shale and that the gas had accumu¬ 
 lated in fractures induced by stimulation. However, the fractures apparently 
 were not extensive enough to constitute an adequate reservoir for commercial 
 production of gas and the well was eventually plugged and abandoned. 
 
 In April, 1975, Frank Norman of Harbor Creek, Erie County, completed a well 
 on his property at a depth of 875 feet in the Devonian shale. The well produced 
 naturally at an open flow rate of 20,000 cubic feet of gas per day from three 
 zones at 150, 400, and 700 feet; enough gas to insure an adequate domestic supply. 
 In December, 1975, St. Joe Petroleum Corporation completed the Ashcroft #1 well in 
 Greene Township, Beaver County. As with the nearby Metropolitan Industry well, 
 the Ashcroft well was originally drilled as a test of a deeper formation (the 
 Lower Silurian Medina Group) but was plugged back to test the Devonian Rhinestreet 
 shale. Again there was no natural production, and after hydraulic fracturing 
 there was no sustained flow. The gas was there, but with the present state of 
 stimulation and recovery techniques it could not be produced economically. This 
 well is currently shut in. 
 
 Nicholas Konzel of Erie, Erie County, drilled a well on his property to a 
 depth of 900 feet. The well was completed in May, 1976, as a shale gas well 
 with a sustained natural flow of 5,000 cubic feet of gas per day, sufficient 
 for domestic use, from the Upper Devonian Dunkirk shale facies. In September, 
 1976, Moody and Associates completed the Welch Foods #3 well in the area of the 
 old North East field as a 900 feet deep Devonian shale test. A natural open 
 
- 5 - 
 
 flow rate of 12,000 cubic feet of gas per day was encountered; after foam frac¬ 
 turing the flow rate was 150,000 cubic feet per day with 80 pounds rock pressure. 
 Piotrowski (1978; also Piotrowski, and others, 1978) reported that a sibilation 
 log run in the well indicated the presence of natural fractures, both in the 
 black shale and the associated gray shale. After a month of testing,the flow 
 rate was reported to have decreased to 3,500 cubic feet per day. The well is 
 currently shut in. 
 
 Henry Oberlander of Erie, Erie County, completed a shale gas well on his 
 property in April, 1977, at a depth of 800 feet. The well had an initial potential 
 of 4,000 cubic feet of gas per day natural production and is being used for 
 domestic purposes. In September, 1977, Michael Tarasovitch completed a well on 
 his property in North East Township, Erie County, that encountered gas in the 
 shales less than 600 feet deep. The initial open flow was gauged at 3,000 cubic 
 feet per day with a rock pressure of 36 pounds. In November, 1977, the General 
 Electric #3 well was completed in Lawrence Park Township, just outside the city 
 of Erie, Erie County. The well was originally drilled to the Medina Group (Lower 
 Silurian) but was plugged back to 1,450 feet and completed as a shale gas well 
 with a natural open flow rate of about 30,000 cubic feet of gas per day. Moody 
 and Associates completed the EBC0 #1 well in November, 1977, as a shale gas well 
 for the EBC0 (Erie Burial Case Company) plant in the city of Erie. This well 
 was drilled to a total depth of 901 feet and had significant shows from three 
 horizons. At 381 feet, an open flow rate of 1,300,000 cubic feet of gas per 
 day was gauged. A second show at 533 feet was gauged at 1,700,000 cubic feet 
 per day, and a third show at 731 feet had a flow rate of 1,300,000 cubic feet 
 per day. After completion of drilling operations, the well was shut in for 
 five days and tested again. This time the natural gas flow was measured at 
 975,000 cubic feet per day. Sibilation and temperature logs run in nearby wells 
 indicate a system of natural fractures serve as the reservoir in the area; this 
 
- 6 - 
 
 would account for the large amounts of gas gauged. Although the actual potential 
 of the well is uncertain, the well is producing enough gas to provide an adequate 
 supply for the needs of the Erie Burial Case Company. Samples of the drill 
 cuttings from the three zones of production were analyzed at the Pennsylvania 
 Geological Survey's research laboratory in Harrisburg by John Barnes of the 
 Survey's Mineral Resources Division. The analysis shows that the mineralogy 
 of the shale was consistent at all three horizons, containing abundant illite 
 and quartz, and less abundant though significant kaolinite, chlorite, feldspar 
 and an illitic mixed-layered clay which is significantly expandable. The presence 
 of these expandable clay minerals is important to the design of the stimulation 
 procedures. These expandable clay minerals could result in closed fractures or 
 even a caved-in hole if hydraulic fracturing using fresh water-based fluids were 
 applied. 
 
 In March, 1978, the U. S. Department of Energy sponsored a massive foam 
 fracture treatment of the Peoples Natural Gas #1 Fleck well in Sandy Creek Town¬ 
 ship, Mercer County. The well had originally been drilled as a basement test but 
 was plugged back to 5,200 feet to test the Devonian Rhinestreet shale. Unfor¬ 
 tunately, a mechanical failure occurred during stimulation, and the well was 
 plugged and abandoned. In May, 1978, the Wayne Corporation completed a shale 
 well in Millcreek Township, Erie County. The well was originally permitted to 
 test the Medina Group (Lower Silurian) but several shows were encountered between 
 15 feet and 1,247 feet and drilling was halted at 1,465 feet. After the well 
 was shut in for 10 days, it was tested and gauged at 363,000 cubic feet of gas 
 per day natural production, an amount sufficient for commercial production. 
 
 Eastern Gas Shale Project 
 
 The U. S. Department of Energy has embarked on an extensive study of the 
 organic-rich black shales of the Appalachian Basin. The purpose of the study 
 is two-fold. The first objective is resource evaluation and research into the 
 
- 7 - 
 
 factors affecting hydrocarbon accumulation in the shales. This objective requires 
 preparation of stratigraphic cross sections; preparation of isopach, lithofacies 
 and structure contour maps; compilation of maps showing wells with production and 
 shows from the black shales; examination of outcrop samples, drill cuttings, and 
 cores to characterize mineralogy, organic content, trace element composition, 
 microfossil content, and physical properties of the rock. These data will be 
 assembled and used to prepare a series of maps and reports indicating the resource 
 base and potential hydrocarbon reserves. The second purpose of the study, 
 technological development, is designed to increase production potential by 
 developing and implementing new drilling, stimulation, and recovery techniques. 
 
 New technology is needed to locate fracture systems and potential reservoirs 
 (geophysical analysis), to investigate ways ,to modify the shale matrix to increase 
 gas flow (geochemical advances), and to derive and test models of various hydraulic 
 and explosive fracturing techniques and directional drilling procedures (engineer¬ 
 ing problems). A listing of all participants in this program, along with a summary 
 of all contracts is available in the report, "Summary of Contracts for Eastern Gas 
 Shale Project," published by the Morgantown Energy Research Center (MERC), Morgan¬ 
 town, West Virginia. 
 
 As one of the participants in this program, the Oil and Gas Geology Division 
 of the Pennsylvania Geological Survey has the responsibility of carrying on a 
 portion of the resource evaluation phase of the project within Pennsylvania. 
 
 The Survey has contracted to provide a stratigraphic and structural framework 
 for the predominantly clastic sediments between the Murrysville-Berea-Cussewago 
 interval (the traditional Mississippian-Devonian boundary as accepted by Kelley 
 and Wagner, 1970) and the top of the Middle Devonian Onondaga Limestone. This 
 includes definition and mapping of the various black shale facies and related 
 rocks within this sequence in order to understand their sedimentological histories 
 and to enable further prediction and evaluation of potential gas resources in the 
 
Devonian shales. 
 
 METHODS 
 
 The Pennsylvania Geological Survey has completed nine stratigraphic cross 
 sections of the Upper Devonian "Catskill" clastic wedge in Pennsylvania (Figure 2). 
 These cross sections are based on gamma ray logs, with some associated sample 
 description logs, at a vertical scale of 1 inch = 100 feet. There are three 
 sections oriented approximately north-south and six oriented approximately east- 
 west forming an enclosed "egg crate" shaped network. 
 
 Gamma ray logs are used as the primary source of data in this study. Almost 
 all of the natural gamma radiation emitted from rocks is due to the radioactive 
 potassium isotope (K^O) found in feldspars, micas, and other common silicate 
 minerals, and to elements of the uranium and thorium series found in minor 
 amounts in sediments. In sedimentary rocks the gamma ray log generally reflects 
 shale content because there is generally a higher concentration of K^O in shales. 
 Non-shaly rocks such as clean sandstones and limestones have very low levels of 
 radioactivity and may, therefore, be differentiated from shales on a gamma ray 
 log. 
 
 Studies of uranium-rich sedimentary rocks indicate that marine black shales 
 have higher than normal radioactivity responses. Adams and Weaver (1958) hypo¬ 
 thesized that this stronger gamma ray response is due to the reduction of uranyl 
 ions in solution to tetravalent uranium ions by organic matter and other reduc- 
 tants. This uranium is then concentrated in the sediments by being fixed in 
 organic complexes, adsorbed on organic material, or adsorbed on clay minerals. 
 
 Many marine black shales have uranium contents greater than 10 parts per million 
 and may approach 100 parts per million. Thus, relatively high gamma ray responses 
 could define organic-rich shales. Sample logs used in conjunction with gamma ray 
 logs can be used to indicate the relationship between high radioactivity and 
 black shales. Figure 3 shows that there is a general correspondence between 
 
Figure 2. Index of cross sections in Pennsylvania. 
 
GAMMA RAY 
 API UNITS 
 
 0 200 
 
 200 400 
 
 Figure 3. Portion of gamma ray and associated sample logs of a hypothetical 
 well showing the method of determining radioactive shale and 50% 
 clean sand cutoffs. See text for discussion. 
 
11 
 
 the two types of logs, the major difference being that the sample log does not 
 adequately define formation boundaries. 
 
 Formation density also has an important effect on gamma radiation readings. 
 Two formations with the same amount of radioactive material but having different 
 densities will show different radioactivity levels on the gamma ray log; the 
 lower density rocks will be more radioactive. Gamma rays are gradually absorbed 
 and their energies are degraded as they pass through rocks; a more dense rock 
 will absorb more gamma rays than a less dense one. Therefore, high radioactivity 
 responses on gamma ray logs may be due to low bulk density caused by changes in 
 composition or fractures in the rock. 
 
 In areas where shale-gas production has been developed and studied, an 
 empirical relationship exists between high radioactive response and gas produc¬ 
 tion from shales. This has been shown by Martin and Nuckols (1976) from wells 
 in the Cottageville Field, Jackson and Mason Counties, West Virginia, and by 
 Bagnall and Ryan (1976) from wells in southwestern West Virginia. Martin and 
 Nuckols plotted gas shows from 37 wells producing from Devonian shales in the 
 Cottageville Field on a typical gamma ray log from the same area. Their diagram 
 shows that the majority of gas production is directly related jto zones having 
 high gamma ray responses. Bagnall and Ryan analyzed well cuttings from a well 
 in Kanawha County, West Virginia, for gas content, and directly correlated total 
 gas content of the cuttings with high radioactivity readings on the gamma ray 
 log from that well. Similar data have been reported by Majchszak (1978) and 
 Smith (1978). 
 
 In Pennsylvania, the geophysical logs and production records from the 
 Metropolitan Industry #1 well in Beaver County and the Welch Foods #3 well in 
 Erie County were analyzed by Piotrowski, and others (1978). Details of the 
 Metropolitan Industry well are shown in Figure 4. The various stratigraphic 
 units and zones of perforation and production are indicated. The logs demonstrate 
 
COLUMBIANA 15 
 
 Beaver County 
 Metropolitan Industry p \ 
 Quaker State 
 El 948 gl 
 
 GAMMA RAY LOG DENSITY RESISTIVITY SONIC 
 
 Shale Gas Discovery 
 
 COLUMBIANA 15 
 
 Figure 4 
 
 Portions of combined geophysical logs of Metropolitan Industry #1 
 well, Beaver County, Pennsylvania, showing zones of shale-gas production 
 
13 - 
 
 that the productive zones correspond to high radioactivity, low density, and 
 high porosity (the latter indicated by the neutron log). The resistivity log 
 shows readings of 100 ohms or greater in the productive zones, probably indicat¬ 
 ing hydrocarbon content; the sonic log cycle-skips in these intervals, perhaps 
 because of natural fractures or gas in the rock. The details of the Welch Foods 
 well logs are shown in Figure 5. Like the Metropolitan Industry well, the Welch 
 Foods well logs show high gamma ray response, low density, high porosity, and 
 high resistivity associated with the gas producing horizons. A sibilation log 
 from this well, by its positive readings, indicates that a system of fractures 
 probably exists in the rock. 
 
 In this study, a shale having a radioactive response greater than 20 API 
 units above a 100% shale base line (Figure 3) is considered a radioactive shale. 
 Twenty API units was chosen as the cutoff because it is thought that this amount 
 is consistently greater than any recognizable mechanical deviation of the logging 
 instruments. Sands were defined on the basis of a 50% clean sand cutoff (Figure 3). 
 A 100% sand base line was chosen by assuming that the lowest gamma ray response 
 on the log represented a very clean sand. Knowing the 100% sand and 100% shale 
 base lines, the 50% sand line can be chosen since the response is linear. With 
 these cutoffs established it is easy to calculate net feet thicknesses, average 
 sand thicknesses, and lithologic ratios. 
 
 The advantages of using gamma ray logs for this type of study are three-fold: 
 (1) gamma ray logs are the most common geophysical log run in wells in Pennsyl¬ 
 vania and they are usually readily available; (2) the radioactivity responses 
 are consistent - the gamma ray log can be used effectively with fluids or casing 
 in the hole; and (3) gamma ray logs are more accurate than sample logs because 
 the logging equipment can give a continuous reading throughout the hole, rather 
 than at 5, 10, or 20 foot intervals. In this way the gamma ray log can be used 
 to pick formational boundaries within several feet, whereas sample descriptions 
 
NORTH EAST B38 
 
 Erie County 
 Welch Food Inc *3 
 Welch Food Inc. 
 
 EL 797 g I 
 
 GAMMA RAY LOG DENSITY RESISTIVITY SIBILATION 
 
 Shale Gas Discovery 
 
 NORTH EAST B38 
 
 ure 5. Portions of combined geophysical logs of Welch Foods #3 well, Erie 
 County, Pennsylvania, showing zones of shale-gas production. 
 
15 - 
 
 cannot. 
 
 The nine completed stratigraphic cross sections (Figure 2) form the basis 
 of this study. The gamma ray logs from approximately 500 wells penetrating the 
 sand and shale sections were correlated to these sections. Logs were chosen so 
 that there would be, where available, at least one data point per five minutes 
 of latitude and longitude throughout the study area. Each log has a designated 
 file number indicating 15-minute quadrangle, reference section, and number as 
 set up by the Pennsylvania Geological Survey Oil and Gas Geology Division (Kelley 
 and Wagner, 1970). Each 15-minute quadrangle is divided into nine 5-minute 
 sections labeled A to I. Therefore, a log labeled Erie B-128 indicates that it 
 is from the 128th well of record in the Erie 15-minute quadrangle and that it is 
 located in section B of that 15-minute quadrangle. 
 
 GENERAL STRATIGRAPHY 
 
 The black, organic-rich shales of Devonian age in Pennsylvania occur at and 
 near the base of a thick, wedge-shaped sequence of sedimentary rocks known in 
 western Pennsylvania by drillers as the "Catskill" clastic wedge. This westward¬ 
 thinning, bevel-edged, sequence of intercalated marine, transitional, and contin¬ 
 ental facies attains a thickness of over 7,000 feet in south central Pennsylvania 
 and thins to about 2,000 feet in the northwestern part of the state. The rocks 
 are most commonly shales, siltstones, sandstones, and red beds, but a few thick 
 limestones are found in the lower part of the sequence. 
 
 The stratigraphic terminology for the Upper Devonian sedimentary sequence 
 in the subsurface of Pennsylvania is confused by contradictions, unit names 
 defined by non-standard procedures, and drillers' units to which conflicting 
 names have been applied. Names such as "Catskill", "Chemung", and "Portage" 
 have been used in a wide variety of ways (see Frakes, 1963, for an excellent 
 discussion of this problem) and it seems that only those units which have been 
 described from outcrop localities in central Pennsylvania have any acceptable 
 
16 - 
 
 status. This paper is, in part, an attempt to initiate a more consistent and 
 
 more meaningful stratigraphic nomenclature for the subsurface Upper Devonian of 
 
 Pennsylvania. The old nomenclature is, if anything, overdeveloped. Most of the 
 
 terminology used in the black shale portion of this study is based on that of 
 
 the New York Geological Survey (Rickard, 1975) modified by the U. S. Geological 
 
 * 
 
 Survey (Oliver, and others, 1969). No attempt has been made to define all of 
 the Upper and Middle Devonian formation members recognized in New York. Fortun¬ 
 ately, most of the formational boundaries are based on marker horizons such as 
 limestones and black shales which are readily distinguishable in the subsurface 
 by their gamma ray responses. 
 
 Black Shale Facies 
 
 Three major and three minor black shale facies are recognized in the subsur¬ 
 face of Pennsylvania. The major units include the Middle Devonian Marcell us 
 facies of the Hamilton Group, and the Upper Devonian Rhinestreet facies of the 
 West Falls Formation and Dunkirk facies of the "Canadaway Group". The minor 
 units are the Burket facies of the Genesee Formation, the Middlesex facies of 
 the Sonyea Formation, and the Pipe Creek facies of the Java Formation, all Upper 
 Devonian. These black shale facies in Pennsylvania and their relationship to 
 the formally recognized units of New York and Ohio are shown in Figure 6. 
 
 At its thinnest the Marcellus facies in the subsurface of Pennsylvania may 
 be equivalent to a portion of the Marcellus Formation of New York, whereas it 
 probably encompasses the total Marcellus and Skaneateles formations and part 
 of the Ludlowville Formation in the area of its greatest accumulation. The 
 Burket facies of the Genesee Formation is equivalent to the Geneseo Shale Member 
 of New York. In the northeastern portion of the study area, the Burket is split 
 into an upper "Renwick" black shale and a lower "Geneseo" black shale separated 
 by non-black shales and siltstones. Geneseo as used by the New York Geological 
 Survey is applied to the lower unit regardless of the presence or absence of the 
 
SERIES STAGE 
 
 TERMINOLOGY 
 
 OHIO 
 
 NEW 
 
 YORK 
 
 NW SE 
 
 RECOGNIZED UNITS IN THE SUBSURFACE OF PENNSYLVANIA 
 
 LOWER 
 
 MISS. 
 
 z 
 
 < 
 
 z 
 
 o 
 
 > 
 
 Ld 
 
 O 
 
 Ld 
 
 J 
 
 O 
 
 Q 
 
 KINDER- 
 
 HOOKIAN 
 
 BEREA 
 
 SS. 
 
 POCONO 
 
 SS. 
 
 MURRYSVILLE-BEREA- CORRY-CUSSEWAGO SANDSTONE 
 
 < 
 
 CL 
 
 Ld 
 
 I p \ 
 
 CL 
 Ld 
 
 LOWEI 
 
 OLEN- 
 
 TANGY| 
 
 SHALE 
 
 DELA-. 
 WARE/ 
 LS J 
 
 tr 
 
 < 
 
 CL 
 
 CO 
 
 V) 
 
 m 
 
 z 
 
 3 
 
 _l 
 
 O 
 
 o 
 
 GENESEE 
 
 
 FM. 
 
 
 TULLY 
 
 
 LS. 
 
 CL 
 
 3 
 
 O 
 
 MOSCOW 
 
 FM. 
 
 cr 
 
 o 
 
 LUDLOW- 
 
 VILLE 
 
 FM 
 
 o 
 
 >— 
 
 _j 
 
 SKANE- 
 
 ATELES 
 
 FM 
 
 < 
 
 X 
 
 MAR- 
 
 CELLUS 
 
 FM. 
 
 ONONDAGA 
 
 LS. 
 
 'IT 1 1 1 1 T 1 1 IT 1 1 IT* 
 
 
 DRILLER'S TULLY OF_ 
 
 N.W. PENNSYLVANIA? V 
 
 -4^4- tully' ij i ; ; 1 ; i ; i ; i !^ b v, rket : 
 
 -II I I IUFQTHM 1 1 I I 1 I ‘ I 1 
 
 1 I 1 I- 1 - 1 -L—L. 
 
 
 l‘l‘| 1 T J -| 1 T^ 
 
 i. i. i. i 
 
 
 ]ONONDAGA 
 J LIMESTONE 
 
 
 it 
 
 i i i i i ~ 
 
 -T, I , 1 . 1 , l 
 
 V i' i 1 1 1 1 ‘ i; i; i 
 
 
 HUNTERSVILLE 
 
 CHERT 
 
 ‘^Li Li | i !e'selinsgrqve IrlijT 1 
 
 rm 
 
 i . i i i i r i 
 
 iii r 
 
 
 5^- 
 
 limestoneV : .! 45 
 
 r i ‘i 1 1 1 1 ‘i ‘1 1 1 1 1 1 1' 
 
 NEEDMORE 
 
 SHALE 
 
 Figure 6. Schematic illustration of Upper and Middle Devonian stratigraphic 
 units in the subsurface of Pennsylvania and correlation with Ohio 
 and New York stratigraphic section (after Oliver, and others, 1909, 
 and Patchen, 1977). 
 
- 18 - 
 
 Renwick. 
 
 The Middlesex facies of the Sonyea Formation in the Pennsylvania subsurface 
 is equivalent to the Middlesex Shale Member of New York, and the Rhinestreet 
 facies of the West Falls Formation corresponds to the Rhinestreet Shale Member 
 of New York usage. The Pipe Creek facies of the Java Formation is a very thin 
 but very persistent black shale recognized at the surface in New York. The 
 black shale identified in the subsurface of Pennsylvania as the Dunkirk facies 
 of the "Canadaway Group" is equivalent to the Dunkirk Shale Member of New 
 York plus a number of superjacent members of the "Canadaway" in those areas 
 of the Dunkirk's greatest accumulation. The Dunkirk, like the Middlesex, 
 Rhinestreet, and Pipe Creek facies, thickens westward from New York through 
 Pennsylvania and into Ohio where it is several hundreds of feet thick and is 
 recognized by the name Huron Member of the Ohio Shale. 
 
 Sand Facies 
 
 The Upper Devonian shallow sand oil and gas reservoirs have been the sub¬ 
 ject of a confusing terminology, originating mostly from drillers who were less 
 interested in the geological consistency and usefulness of stratigraphic nomen¬ 
 clature than they were in the amount of oil and gas produced from a reservoir. 
 Names were liberally applied to sandstones and conglomerates at many localities 
 of first discovery and these names were carried over long distances where they 
 were commonly applied to non-equivalent sands. Certain of the sands appear to 
 be continuous, but gamma ray correlations indicate that the majority of drillers 
 terms define belts of sand and silt lenses, rather than individually mappable 
 units. In an attempt to create some order out of the chaos, Kelley and Wagner 
 (1970) defined a number of zones which represent "bundles" of drillers' "sands". 
 
MISSIS¬ 
 
 SIPPI 
 
 AGE 
 
 ? 
 
 o 
 
 LU 
 
 O 
 
 ct: 
 
 UJ 
 
 Q- 
 
 ZONES 
 
 UNITS 
 
 SAND NAMES 
 
 
 Big Injun 
 
 Loyalhanna 
 
 Big Injun-Mountain 
 
 Burqoon 
 
 MIDDLE AND 
 
 LOWER 
 
 P0C0N0 
 
 
 Shenango, Slippery Rock, Squaw 
 
 Second Gas 
 
 Berea, Cussewago, Corry, Knapo, Murrvsville 
 
 RICEVILLE 
 
 
 Riceville Shale in north central Pennsylvania 
 
 
 D 3 
 
 Venango First, Hundred Foot, Fifty Foot, Gantz, 
 Drake, Tuna 
 
 Red Valley, Lytle, Rosenberry, White, Salamanca 
 
 D 
 
 UPPER SAND 
 ZONE 
 
 D 2 
 
 Venango Second, Salt, Upper Nineveh, Lower 
 
 Nineveh, Snee, Shira, Boulder 
 
 Venango Third Stray, Venango Third, Venango 
 Fourth (Fourth), Venango Fifth (Fifth), 
 
 Venango Sixth (Sixth), Grey, Black, Green, 
 Gordon Stray, Gordon, McDonald Fourth, 
 
 McDonald Fifth, Knox Third Stray, Knox Third, 
 Knox Fourth, Knox Fifth, Wolf Creek, Clarion, 
 Byram, Conewango, LeBoef, Maqee Hollow 
 
 
 D 1 
 
 Bayard 
 
 Elizabeth 
 
 C 
 
 SHALE ZONE 
 
 
 
 
 B 4 
 
 Warren First 
 
 Warren Second 
 
 Queen 
 
 Glade, Bradford First, Eighty Foot, 
 
 Clarendon Stray 
 
 B 
 
 B 3 
 
 Clarendon, Sugar Run, Watsonville, Dew Drop, 
 
 Chipmunk, Cherry Grove, Gartland, Upper 
 
 Ball town. Lower Balltown, Speechley 
 
 MIDDLE 
 
 SAND ZONE 
 
 B 2 
 
 Tiona, Cooper Stray, Cooper 
 
 Bradford Second 
 
 Klondike, Harrisburg Run 
 
 Deerlick, Slivervilie 
 
 
 B 1 
 
 Bradford Third 
 
 • Lewis Run 
 
 Upper Kane 
 
 Lower Kane 
 
 Sartwel1 
 
 Bo 
 
 LOWER SAND 
 ZONE 
 
 Undivided 
 
 Haskil1, Reily, Elk 
 
 Humphrey, Benson, Alexander 
 
 Figure 7. Generalized stratigraphic column of producing sandstones in the Upper 
 Devonian of western Pennsylvania. Placement of sand names within a 
 zone refers only to the position of, the sand in the area where it was 
 first named or used. 
 
20 - 
 
 We have accepted their zonation with modification (Figures 6 and 7). In this 
 study, Zones D, B, and Bo represent three identifiable "bundles" of sands which 
 are further subdivided on the basis of the drillers' terminology, while Zones A 
 and C are shale facies. The zones are believed to be correctable lithologic 
 divisions which may be formally named in the future. 
 
 Zone A is a very general division. It represents all of the non-black shales 
 and shaly siltstones which lie above the top of the highest definable black shale 
 facies and below the base of the lowest identifiable sand (Figure 6). In Erie 
 County where the shallow sands are absent. Zone A includes all of the sedimentary 
 rocks from the top of the Dunkirk facies to the base of the overlying Mississippian 
 rocks (or to the surface in areas where the Mississippian has been eroded). In 
 Somerset County, however. Zone A encompasses all of the sediments lying between 
 the top of the Burket facies and the base of sandstone Zone Bo. Zone C and the 
 Riceville Shale (Figure 6) are tongues of Zone A which are intercalated with the 
 sandstone "bundles" of Zones D and B and the basal sandstones of the Mississippian 
 Pocono Group. 
 
 The unit designations B1, B2, B3, B4, and D1, D2, D3 within lithic Zones B 
 and D (Figure 7) are interval divisions rather than lithologic division. This 
 is done in an attempt to show the relationship between drillers' terminology 
 and stratigraphic units. These divisions are based on the positions of the 
 known producing "sands" (belts of discontinuous and non-correlatable sandstone 
 lenses) as first named by oil and gas drillers. Placement of the sand within 
 each unit designation refers only to the position of that sand in the area where 
 it was first named. Zones D and B are separated by the shale Zone C. In the 
 areas where it is less than 50 feet thick. Zone C cannot adequately be differen¬ 
 tiated from the interbedded shales within the sand zones. At this point Zones B 
 and D coalesce and, with Zone Bo, become a single sandstone Zone D-B-Bo (Figure 6). 
 Zone Bo is best developed in the eastern portion of the study area where sandstones 
 
and siltstones develop below the limit of Zone B as recognized elsewhere. 
 
 DISCUSSION OF THE MAPS 
 
 General 
 
 This portion of the report attempts to describe the import of the structural, 
 isopach, and lithofacies data presented in the accompanying 39 maps. Twenty-two 
 of these maps are based on the Upper and Middle Devonian radioactive black shales 
 and their associated lithologies. The remaining 17 maps deal with the Upper 
 Devonian sandstone zones and intercalated shale zones. Interpretation of these 
 maps is based not only on the maps themselves, but also on individual gamma ray 
 logs and numerous cross sections prepared during the mapping phase of the study. 
 
 Black Shale Maps 
 
 A. Total Interval from Top of Devonian to Base of Marcellus 
 
 The total interval from the Mississippian-Devonian boundary to the base 
 of the Marcellus shale facies exhibits the pattern of southeastward thicken¬ 
 ing (Plate 1) which is character!'Stic of most of the individual units within 
 it. Major changes in the gradual basinward thickening of these units are 
 rare. The map of the net feet of radioactive black shale in the total 
 interval (Plate 2) shows a linear pattern of thick and thin areas which seem 
 to be related to the general northeast-southwest strike of the Appalachian 
 structures. This map is a composite of all of the radioactive shale facies 
 and it shows, in general, the trends associated with them. It especially 
 depicts the three major shale belts in Pennsylvania. The Marcellus belt 
 in the eastern portion of the study area is represented by the isolated 
 thick areas of 150 net feet or greater in the southeast and the broad con¬ 
 tinuous pattern of greater than 150 net feet thickness in the northeast. 
 
 The Rhinestreet and Dunkirk belts are represented by the northwestern trends 
 of 150 net feet or greater thickness, with the Dunkirk belt occupying the 
 
22 
 
 Lake Erie margin and the Rhinestreet belt lying somewhat to the southeast 
 of it on a line from Beaver to Warren Counties. The small, isolated thick 
 area in McKean County is the result of local thickening of organic-rich 
 shale. 
 
 B. Middle Devonian 
 1. Hamilton Group 
 
 The Hamilton Group in the subsurface of Pennsylvania is divided 
 into the lower Marcellus shale facies and the superjacent Mahantango 
 Formation which is equivalent to the Skaneateles, Ludlowville, and 
 Moscow formations of New York (Figure 6). The Hamilton Group isopach 
 map (Plate 3) indicates the general thickening trend shown in Plate 1. 
 However, it should be noted that there is a slight change in the spacing 
 of the contour lines at approximately the 500 foot line. To the south¬ 
 east, especially in the center of the study area, the contours are more 
 closely spaced, while to the northwest they open up. The isolated 500 
 foot contour in central McKean County is the result of a single well in 
 which the Onondaga equivalent sediments are radioactive black shales, 
 adding about 100 feet to the lower portion of the Hamilton Group. 
 
 The Map of net feet of radioactive black shale in the Hamilton Group 
 (Plate 4) shows the eastern belt of black shales delineated in Plate 2. 
 Using an arbitrary 125 net feet of shale as a cutoff between low and 
 high values, the Marcellus develops into a series of linear thickened 
 areas paralleling the structural axes. Comparison of this map with 
 that of the structure on top of the Onondaga Group (Plate 5) indicates 
 that the majority of these thickened areas are developed on the crests 
 of anticlines. Harper and Piotrowski (1978) proposed that the structures 
 in this area were probably active tectonic features throughout much of 
 the Devonian. The anticlines, therefore, would have been positive 
 
23 - 
 
 features at the time of deposition of the Marcellus black shale. Stag¬ 
 nant, anaerobic conditions could then occur within the organic-rich 
 sediments accumulating on these features if current activity were 
 restricted to the low areas between the crests. These currents would 
 serve the double purpose of aerating and winnowing the sediments in 
 the troughs, and isolating patches of anaerobic conditions on the anti¬ 
 clines. We hope to study this problem in the future to determine if, 
 in fact, this is a valid hypothesis for the origin of the linear thick¬ 
 ness highs. 
 
 The near coincident patterns of the Marcellus facies map and of the 
 Onondaga structure map indicate a change in Marcellus facies thickness 
 and structural complexity along the same line between Greene and Potter 
 Counties. This correlates with the change in contour interval of 
 Hamilton thickness as previously stated. 
 
 2. Tully Limestone 
 
 The Tully Limestone isopach map (Plate 6) corresponds well with the 
 previously published map of Jones and Cate (1957, Plate 6). We have 
 added some modifications, but it is significant to note the similarities 
 between the older map interpreted from well-cutting data and our Plate 6 
 interpreted from gamma ray logs. We agree with Jones and Cate that the 
 Tully Limestone occurs, and indeed thickens, in northwestern Pennsylvania, 
 contrary to the ideas presented by Heckel (1969, 1973) and Wright (1973) 
 and repeated by other authors (for example, Dennison and Head, 1975). 
 
 Areas where the limestone is absent occur in the western part of Lawrence 
 and Mercer Counties and in portions of Warren and McKean Counties, but we 
 can find no reason for calling the thick Middle Devonian carbonates in 
 Venango, Crawford and Erie Counties anything but Tully. We have examined 
 a correlated section of gamma ray logs extending up-dip from the known 
 
24 - 
 
 Tully outcrop in central Pennsylvania to the subsurface of Erie County 
 (Louis Heyman, unpublished cross section, 1978) and see no evidence for 
 the unconformity usually indicated in place of the Tully (Wright, 1973; 
 also Wallace, and others, 1977; and Roen, and others, 1978). 
 
 A linear area of thick Tully, extending from Fayette County into 
 Westmoreland County, lies along the crest of the Chestnut Ridge anti¬ 
 cline. To the east of this area, the Tully becomes less calcareous 
 and eventually disappears as a limestone along a line corresponding 
 to the crest of the Laurel Hill anticline. The Tully is not eroded 
 here, but has undergone a lateral change from a carbonate to a cal¬ 
 careous shale. We surmise from this that the Laurel Hill anticline was 
 
 A 
 
 an active positive feature which became an effective shield against 
 clastic influx from the southeast by slowing water movement over it. 
 
 On the crest and to the east of this structure, carbonate deposits were 
 diluted with fine-grained elastics which were no longer carried in sus¬ 
 pension. On the west side of the anticline, carbonate deposition was 
 essentially undiluted by clastic influx. The Chestnut Ridge anticline 
 may also have been positive and, if the water depth over these two 
 structures was shallow enough, thicker accumulations of carbonates 
 would be deposited on a postulated "Chestnut Ridge carbonate platform" 
 accounting for the pattern seen on the map. 
 
 Another thick area of Tully Limestone occurs along the Allegheny- 
 Westmoreland County boundary and extends northeastward. We have no 
 immediate explanation of this feature. 
 
 The Tully Limestone is relatively thick in the southeast and thins 
 to the northwest. This change occurs where structural changes occur, 
 along a line from Greene County to Potter County (Plate 7). The structure 
 on the top of the Tully is essentially the same as that on the top of the 
 
25 - 
 
 Onondaga Group (Plate 5) indicating that there was little apparent 
 tectonic activity during the Middle Devonian. 
 
 C. Upper Devonian 
 
 The isopach of total Upper Devonian shale (Plate 8) reflects the distri¬ 
 bution of shale from the top of the Tully Limestone, or its equivalent, to 
 the base of the first sand (shale Zone C and the Riceville Shale are not 
 included). In northwestern Pennsylvania, the shale is relatively thin (less 
 than 3,000 feet) due to the general thinness of the total section. In the 
 central portion of the study area, the alternating thin and thick belts are 
 apparently partially related to the distribution of Zone B Sandstone (see 
 Plate 27). The easternmost belt of thin shale lies along the area in which 
 the Zone Bo and Zone B sands (Plates 25 and 27 respectively) are best 
 developed. 
 
 The total net feet thickness of radioactive black shales in this interval 
 (Plate 9) shows that the thickest Upper Devonian black shale is found in 
 northwestern Pennsylvania. This distribution of greater than 100 net feet 
 of shale is due in most part of the presence of the Dunkirk and Rhinestreet 
 facies. 
 
 1. Genesee Formation 
 
 The Genesee Formation, like the Hamilton Group, gradually thickens 
 toward the southeast. In extreme northwestern Pennsylvania the Genesee 
 Formation is missing, apparently having been pinched out or eroded from 
 the area. A noticeable change in rate of thickening occurs at about 
 the 100 foot contour line (Plate 10). To the east, the superjacent 
 Middlesex radioactive shale facies of the Sonyea Formation changes 
 character by dilution of the organic-rich shale with non-organic elastics. 
 Where it disappears the Genesee Formation can no longer be defined. 
 
- 26 - 
 
 However, the individual radioactive shale members within the Genesee 
 can still be distinguished. 
 
 The Burket radioactive shale facies is identifiable throughout most 
 of the study area, although it pinches out in northwestern Pennsylvania 
 (Plate 11). To the east, the Burket thickens gradually until, in the 
 central portion of the study area, thickening becomes more rapid. At 
 about the 50 foot contour line the Burket splits to become the upper 
 Renwick facies and the lower Geneseo facies (Figure 6) separated by 
 unnamed non-radioactive shales and siltstones. The distribution of 
 these rocks is quite different from the distribution of other units 
 in the Devonian of Pennsylvania. The Burket-Geneseo-Renwick interval 
 attains its maximum development in the northeastern, rather than south¬ 
 eastern portion of the study area, implying a radically different source 
 area for the organic-rich elastics. This is also implied by the net feet 
 of radioactive shale from this interval (Plate 12) which has its maximum 
 distribution in the northeast. While most of the Upper and Middle 
 Devonian clastic input was from the southeast, the lower Genesee members 
 were apparently formed by a shift in the center of deposition to the 
 northeast, with provenance from what is now New York State. 
 
 2. Sonyea Formation 
 
 The Sonyea Formation thickens to the southeast (Plate 13) in a manner 
 similar to that of the Hamilton Group and the Genesee Formation. In 
 extreme northwestern Pennsylvania the Sonyea, like the Genesee, is 
 absent. The superjacent Rhinestreet radioactive shale facies of the 
 West Falls Formation is absent in the central portion of the study area, 
 but a distinctive marker at the base of the Rhinestreet persists further 
 toward the southeast. Where the Rhinestreet marker can no longer be 
 picked, the Sonyea Formation can no longer be recognized as a mappable 
 
27 - 
 
 lithologic unit. The lower member of the Sonyea, the Middlesex radio¬ 
 active shale facies, can be traced only a little farther east before it 
 too dies out (Plate 14). 
 
 The Middlesex is rarely identified in the subsurface of Pennsylvania 
 as a thick radioactive shale unit, although Sutton (1963) noted that it 
 is approximately 160 feet thick in south central New York along the 
 Pennsylvania-New York border. Although the Middlesex facies may be over 
 100 feet thick in some areas of Pennsylvania, only in McKean and Potter 
 Counties does it attain a thickness of greater than 25 net feet of radio¬ 
 active shale (Plate 14). This distribution is similar to the Burket- 
 Geneseo-Renwick facies distribution. 
 
 The structure contour map on the base of the Middlesex shale (Plate 
 
 15) shows that the shale has a gentle southeasterly dip northwest of the 
 area of major structures in the subsurface. Here, the base of the Middle¬ 
 sex becomes structurally more complex, forming an asymmetrical syncline 
 with a gentle western slope and a contorted and more steeply dipping 
 eastern slope. Unfortunately, the Middlesex radioactive shale becomes 
 diluted and thereby unidentifiable from other elastics in this eastern 
 area so that the structural picture on the eastern side of the study 
 
 area is obscured. 
 
 3. West Falls Formation 
 
 The West Falls Formation gradually thickens to the southeast (Plate 
 
 16) . It can no longer be identified, however, where the superjacent 
 Pipe Creek radioactive shale facies of the Java Formation disappears. 
 
 The limit of the West Falls occurs in the central portion of the study 
 area. 
 
 The Rhinestreet radioactive shale facies is identifiable to about 
 the center of the study area, but a Rhinestreet "marker" which extends 
 
28 - 
 
 farther to the southeast can be distinguished on gamma ray logs. This 
 marker cannot be considered as part of the measurable facies thickness 
 because it does not contain any radioactive shale, using the accepted 
 definition of the 20 API unit cutoff. The net feet distribution of 
 Rhinestreet shale in Pennsylvania (Plate 17) indicates that the Rhine- 
 street is most well developed in a northeasterly striking belt extending 
 from Beaver and Lawrence Counties to Warren and Erie Counties. It is 
 confined to the northwest portion of the state (northwest of a line 
 between Greene and Potter Counties), whereas the Marcell us facies of 
 the Hamilton Group is most well developed to the southeast of this line 
 (Plate 4). 
 
 The structure on the base of the Rhinestreet facies and marker 
 (Plate 18) is quite similar to that of the Middlesex. The base of the 
 shale dips gently to the southeast as far as the line from Greene County 
 to Potter County at which point the structure becomes somewhat more com¬ 
 plex, forming a syncline. The Rhinestreet marker can no longer be 
 identified in the eastern portion of the study area, and this obscures 
 the structural picture in this area. 
 
 4. Java Formation 
 
 The Java Formation thickens gradually to the southeast, but quickly 
 becomes unidentifiable where its upper boundary, the Dunkirk radioactive 
 shale facies of the "Canadaway Group", can no longer be recognized 
 (Plate 19). Because the radioactive shales of the Java Formation never 
 achieve a net feet thickness greater than 20 feet, we have not included 
 a map of this distribution. The structure on the base of the Pipe Creek 
 radioactive shale facies (Plate 20) indicates that it dips gently to 
 the southeast, at least as far as the limit of the radioactive shale. 
 
29 - 
 
 5. Dunkirk Radioactive Shale Facies 
 
 The Dunkirk radioactive shale facies is the basal member of a group 
 of rocks traditionally referred to as the "Canadaway Group". However, 
 we cannot recognize the "Canadaway Group" in the subsurface of Pennsyl¬ 
 vania because its upper boundary cannot be picked on a gamma ray log. 
 
 This boundary is considered by Tesmer (1963) to be marked by the first 
 appearance of gray siltstones containing distinctive fossils character¬ 
 istic of the superjacent "Conneaut Group". By this definition the 
 contact is a biostratigraphic, rather than a 1ithostratigraphic, boundary. 
 Therefore, the "Canadaway Group" by Tesmer's definition, is not based on 
 any mappable lithologic units and cannot stand as a 1ithostratigraphic 
 entity. Rickard (1975) places the contact between the "Canadaway" and 
 "Conneaut" groups as the base of the Dexterville Formation which, accord¬ 
 ing to Tesmer, is not lithologically distinct from subjacent rocks. The 
 U. S. Geological Survey does not use the name "Canadaway Group", prefer¬ 
 ring instead to use individual formation and member names (Oliver, and 
 others, 1969). The Dunkirk, according to this preference, is the basal 
 member of the Perrysburg Formation which has as its upper boundary the 
 Laona Sandstone. Unfortunately, we have been unable to trace the Laona 
 very far in Pennsylvania. It appears to be one of the sand and silt 
 lenses of Zone B or Zone Bo which grades laterally into siltstones and 
 shales indistinguishable from surrounding sediments in northwestern 
 Pennsylvania. We have retained the name "Canadaway" here only for the 
 sake of simplicity realizing that its history is filled with nomenclatural 
 confusion. 
 
 The Dunkirk radioactive shale facies is limited in its distribution 
 to the northwestern part of Pennsylvania. The greatest net feet thick¬ 
 ness of radioactive shale (Plate 21) in this facies is restricted to 
 
30 - 
 
 Erie County essentially paralleling the margin of Lake Erie with a 
 prominent north-south thick tongue, which almost exactly coincides 
 with the thick "Tully Peninsula" (Plate 6) and with the area of the 
 thickest accumulation of Rhinestreet facies (Plate 17). The structure 
 on the base of the Dunkirk (Plate 22) dips gently to the southeast. 
 
 Sand Maps 
 
 The Upper Devonian sandstones are generally distributed as bar-like and 
 channel-like lenses in the subsurface of Pennsylvania. Some of the sandstones 
 and siltstones of Zone Bo are believed to be turbidites. The bar and channel 
 patterns of sand distribution also show up in the isopach maps and maps of net 
 feet of sand of the individual zones and their subdivisions (Plates 23-32, 34-38). 
 Differences in distribution of the sand appear to be due mostly to transgressive 
 and regressive phases of the Devonian seas. 
 
 The three sand zones (Figure 6) represent successively more westward prograda- 
 tional phases of the Upper Devonian "Catskill" clastic wedge. Zone Bo is restricted 
 to the eastern part of the study area (Plate 25), Zone B is generally limited to 
 the east of longitude 80° W (Plate 27), and Zone D almost extends into Ohio (Plate 
 34). The sands of Zone Bo may be mostly turbidites as suggested by their gamma 
 ray log responses (sharp basal contacts and gradational upper contacts; and log 
 indications of "dirty" sands), and the general geometry of the zone in terms of 
 net feet of sand (Plate 26). We believe that at least a portion of Zone Bo can 
 be correlated with the Benson sands of West Virginia, sediments which have been 
 shown to be turbidite deposits (Cheema, and others, 1977). These sands are 
 probably equivalent in part to the Dunkirk radioactive shale facies in north¬ 
 western Pennsylvania (Figure 6) and may be equivalent to other lower black shale 
 facies which die out in the western part of the state. 
 
 Zone B Sandstone contains the Glade, Speechley, Balltown, and Bradford Third 
 sands of drillers' terminology among others (Figure 7), all of which are highly 
 
31 
 
 productive gas and oil reservoirs in the northern part of the study area and to 
 a limited extent in the south. The Speechley is the most widespread sand belt 
 in Zone B. It may be a fairly continuous sand, but unpublished studies of the 
 Speechley (W. R. Wagner, personal communication, 1974) suggest that it is more 
 likely an anastomosing series of coalesced channel or bar-finger sands. The 
 isopach and net feet of sand maps of Zone B (Plates 27-32) indicate that most 
 of the sands were deposited in channel and bar patterns, while distribution of 
 red beds in this interval (the red beds of Zone B are restricted to the eastern 
 portion of the study area) suggests that the majority of Zone B sand was deposited 
 under marine conditions. 
 
 The isopach map of Zone C shale (Plate 33) is interesting in that it shows 
 the same general sort of patterns as the sand maps, with the shale increasing 
 toward the west. The zero contour line coincides with the limit of the individual 
 sand zones, for it is along this line that the Zone D and B sands coalesce. The 
 western limit of Zone C shale is defined by the disappearance of Zone B (Figure 6). 
 
 Zone D Sandstone, containing among others the Hundred Foot, Venango, Gordon, 
 and Bayard sands of drillers' terminology, is a combination of bar and channel 
 patterns (Plates 34-38), more so than the Zone B sandstone. Zone D2 (Plate 37) 
 represents the farthest westward extent of coarse elastics in the Upper Devonian. 
 Most of the wells examined in this study penetrated red beds as well as sands 
 in Zone D2 indicating that the "Catskill" facies of continental sediments also 
 had its farthest westward extent in this interval. These sands are probably 
 very near-shore marine and non-marine sediments. Zone D2 continues to maintain 
 its interval thickness in the east, but the net feet of sand map (Plate 37) shows 
 that the sands within the interval become less developed and eventually lost. 
 
 The shales and siltstones which replace the sands in this section are mostly 
 red or reddish-brown in color, another indication of the continental facies 
 progradation. 
 
32 - 
 
 The Riceville shale is the last effort of the Devonian seas to transgress 
 onto the near-shore marine and continental facies of Zone D. The distribution 
 of the Riceville shale is restricted (Plate 39). It is intercalated with Zone D 
 and the basal Mississippian sandstones approximately along a line between Greene 
 County and Potter County. 
 
 General Stratigraphic Observations 
 
 During the course of mapping, it became apparent that there was evidence of 
 a geological feature associated with, and possibly controlling, the distribution, 
 thickness, structural trends, and facies variability of the Middle and Upper 
 Devonian rocks in the subsurface of western Pennsylvania. This phenomenon is 
 expressed in many of the maps as a broad zone extending from Greene County in 
 the southwest to McKean and Potter Counties in the northeast, parallel to the 
 major structural trend of the Valley and Ridge Province in central Pennsylvania. 
 
 We noticed that the Dunkirk and Rhinestreet facies limits lay along the approxi¬ 
 mate boundaries of this zone (Plates 17 and 21) and could, therefore, be used to 
 delineate it. Other features related to this zone include: change in the contour 
 interval of the Hamilton Group isopach map (Plate 3); restriction of the thickest 
 accumulation of the Marcellus facies to the eastern portion of the study area 
 (Plate 4); distribution of the Tully Limestone (Plate 6); isopach of the total 
 Upper Devonian shale (Plate 8); total net feet of radioactive shale in the 
 Upper Devonian (Plate 9); isopachs of the West Falls Formation (Plate 16) and 
 Java Formation (Plate 19); structure on the various units (Plates 5, 7 and 18 
 especially); and isopachs of the Zone Bo Sandstone (Plate 25), Zone B Sandstone 
 (Plate 27), and the Riceville Shale (Plate 39). 
 
 Figure 8 illustrates some of the more interesting structural and strati¬ 
 graphic features associated with this Greene-Potter zone. The three major 
 radioactive shale facies, Marcellus, Rhinestreet, and Dunkirk, form three broad 
 belts in western Pennsylvania (Figure 8A). The Marcellus attains its greatest 
 
Distribution of the three major radioactive B. Location of postulated Late Cambrian growth 
 
 shale facies. faults of Wagner (1976). 
 
 c 
 
 tO ' 
 
 -o I-''* 
 
 i— 
 
 OJ cr> 
 
 • i— i— 
 
 4— 
 
 €S 
 
 to xz 
 to cn 
 cn o 
 
 -o rd 
 c CQ 
 <d 
 
 •O 
 
 to o 
 s- 
 
 4— 4— 
 O —' 
 
 C. a 3 
 O *1- 
 
 •r- C 
 +-> fd 
 3 > 
 
 -Q r— 
 
 •r- 
 
 S- to 
 4-> C 
 
 to c 
 
 •I- O) 
 Q Cl. 
 
 Q 
 
 Figure 8. Distribution of various structural and stratigraphic features in the subsurface of Pennsylvania and their 
 relationshio to the Greene-Potter zone (bounded by heavy lines). 
 
34 - 
 
 thickness east of the Greene-Potter zone while the Rhinestreet and Dunkirk are 
 best developed to the west. The postulated Cambrian and Ordovician growth 
 faults of Wagner (1976) lie along the margins of the zone (Figure 8B). Distri¬ 
 bution of the sands of the Oriskany Group appear to be related as well (Figure 8C) 
 being absent in the area of the Greene-Potter zone. Distribution of the shallow 
 Devonian oil and gas fields (Figure 8D) is probably also influenced by this 
 phenomenon, either directly or indirectly. Other published data indicate similar 
 relationships throughout geologic time (e.g. reef trends reported by Piotrowski, 
 1976a and 1976b, in the Onondaga Group in McKean County). 
 
 Woodward (1961) seems to be the first to have noticed structural trends of 
 this sort in the subsurface. He proposed a Lower Cambrian "coastal declivity" 
 in western West Virginia that may have continued northeast into Pennsylvania. 
 Wagner (1976) postulated a series of Late Cambrian and Ordovician growth faults 
 which delineated a Late Cambrian trough called the 01in Basin. The axis of the 
 01in Basin approximately coincides with the axis of the Greene-Potter zone. 
 
 Harris (1978) referred this zone to the northern portion of the Eastern Interior 
 Aulacogen which includes the Rome Trough of Kentucky and West Virginia. Root 
 (personal communication, 1978) suggests numerous data supporting the existence 
 of a proposed Greene-Potter fault zone, including some of the evidence presented 
 here. We feel that use of the term fault zone is premature as there is no 
 substantiated evidence of faulting within the zone. 
 
 It is not our objective to attempt to explain the Greene-Potter zone. We 
 simply point out that the distribution of facies, and net feet thicknesses of 
 those facies, appear to bear some relationship to the zone. This phenomenon 
 requires further study and detail before any hypotheses can be made concerning 
 its origins and its relationship to structural and stratigraphic features in 
 the geologic record. 
 
35 - 
 
 SUMMARY 
 
 1. The Devonian organic-rich, radioactive, black shales of Pennsylvania 
 are known producing reservoirs of natural gas (and to a limited extent, oil) 
 which have been exploited in the past. Only recently has interest been renewed 
 in these shales. 
 
 2. It has been shown by several workers that an empirical relationship 
 exists between high gamma ray response on a geophysical log and gas production 
 from shales. High gamma ray response is probably a result of concentration of 
 uranium in the organic matter of black shales. 
 
 3. The relatively greater production of natural gas from the Dunkirk radio¬ 
 active shale facies than from the Rhinestreet and Marcellus facies is a direct 
 result of extensive natural fractures of the rock in the area of Dunkirk shale 
 distribution (Erie and Crawford Counties). Exploration and production have been 
 economically more feasible with regard to the Dunkirk because of shallower drilling 
 depths. 
 
 4. Three major black shale facies exist in the subsurface of Pennsylvania: 
 
 (1) the Marcellus facies of the Hamilton Group, (2) the Rhinestreet facies of 
 the West Falls Formation, and (3) the Dunkirk facies of the "Canadaway Group". 
 
 5. The Upper Devonian sandstone oil and gas reservoirs are divided into 
 three zones representing "bundles" of sandstone lenses which are distributed in 
 bar and channel patterns. These zones, which are intercalated with zones of 
 shale, represent three progradational phases of the Devonian clastic wedge with 
 each zone extending farther to the northwest than the preceeding one. 
 
 6. The three major radioactive shale facies are distributed in northeast- 
 southwest striking belts which may be related to a zone lacking significant 
 radioactive shale thickness extending from Greene County to McKean and Potter 
 Counties (the suggested Greene-Potter fault zone of Root). The Marcellus is 
 most well developed east of this zone, and the Rhinestreet and Dunkirk are 
 
confined to the west of it. 
 
 ACKNOWLEDGEMENTS 
 
 We thank Ms. Patricia Book, Ms. Judy Bugrin, Mr. Lee Golden, Mr. Phillip 
 Golden, Ms. Rhonda Patterson, Ms. Karen Perry, and Ms. Ann Tasillo who aided in 
 the collection, processing, encoding, and plotting of well* data. Mr. John Petro 
 drafted the maps; Mr. Lajos Balogh, Mr. John Petro, and Ms. Patricia Book 
 assisted in preparation of text figure illustrations. Dr. Louis Heyman and 
 Ms. Kathleen Abel reviewed the maps and the text. Ms. Beth Eberst typed the 
 manuscript. Support for this project was provided by the U. S. Department of 
 Energy under contracts E(40-1 )-5198 and EY-76-S-05-5198. 
 
37 - 
 
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 Adams, J. A. S., and Weaver, C. E., 1958. Thorium-to-uranium ratios as indica¬ 
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 Ashley, G. H., and Robinson, J. F., 1922. The oil and gas fields of Pennsyl¬ 
 vania: Pa. Geol. Survey, 4th Ser., Min. Res. Rept. M-l, 78 d. 
 
 Bagnal, W. C., and Ryan, W. M., 1976. The geology, reserves, and production 
 characteristics of the Devonian shale in southwestern West Virginia i_n 
 Devonian Shale Production and Potential: Proc. 7th Appalachian Petrol. 
 
 Geol. Symp., MERC/SP-76/2, Morgantown, WV, p. 41-53. 
 
 Cheema, M. R., Donaldson, A. C., Heald, M. T., and Renton, J. J., 1977. Gas- 
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 central West Virginia (Abs.): Amer. Assoc. Petroleum Geologists Bull., 
 v. 61, p. 775, 776. 
 
 Dennison, J. M., and Head, J. W., 1975. Sea level variations interpreted from 
 the Appalachian Basin Silurian and Devonian: Amer. Jour. Sci., v. 275, 
 p. 1089-1120. 
 
 Frakes, L. A., 1963. Stratigraphy of the non-red Upper Devonian across Pennsyl¬ 
 vania i_n Shepps, V. C., ed.. Symposium on Middle and Upper Devonian strati¬ 
 graphy of Pennsylvania and adjacent states: Pa. Geol. Survey, 4th Ser., 
 
 Bull. G-39, p. 189-199. 
 
 Harper, J. A., and Piotrowski, R. G., 1978. Stratigraphy, extent, gas produc¬ 
 tion, and future gas potential of the Devonian organic-rich shales in 
 Pennsylvania: Preprints, 2nd Eastern Gas Shales Symp., METC/SP-78/6, v. 1, 
 Morgantown, WV, p. 310-329. 
 
 Harris, L. D., 1978. The Eastern Interior Aulacogen and its relation to Devonian 
 shale gas production: Preprints, 2nd Eastern Gas Shales Symp., METC-SP-78/6, 
 v. 2, p. 55-72. 
 
38 - 
 
 Heckel, P. H., 1969. Devonian Tully Limestone in Pennsylvania and comparison 
 to type Tully Limestone in New York: Pa. Geol. Survey, 4th Ser., Inf. 
 
 Circ. 60, 33 p. 
 
 Heckel, P. H., 1973. Nature, origin, and significance of the Tully Limestone: 
 
 Geol. Soc. America, Spec. Paper 138, 244 p. 
 
 Jones, T. H.. and Cate, A. S., 1957. Preliminary report on a regional strati¬ 
 graphic study of Devonian rocks of Pennsylvania: Pa. Geol. Survey, 4th 
 Ser., Spec. Bull. 8, 5 p. 
 
 Kelley, D. R., and Wagner, W. R., 1970. Surface to Middle Devonian (Onondaga) 
 stratigraphy: Pa. Geol. Survey, 4th Ser., Open File Rept. 1. 
 
 Majchszak, F. L., 1978. Preliminary assessment of the applicability of hot¬ 
 wire gas-detection units to exploration and development of Devonian shale 
 gas resources: Preprints, 2nd Eastern Gas Shales Symp., METC/SP-78/6, v. 1, 
 Morgantown, WV, p. 207-218. 
 
 Martin, P. , and Nuckols, E. B., Ill, 1976. Geology and oil and gas occurrence 
 
 in the Devonian shales: northern West Virginia i_n Devonian Shale Production 
 and Potential: Proc. 7th Appalachian Petrol. Geol. Symp., MERC/SP-76/2, 
 Morgantown, WV, p. 20-40. 
 
 Oliver, W. A., deWitt, W., Jr., Dennison, J. M., Hoskins, D. M., and Huddle, J. W., 
 1969. Correlation of Devonian rock units in the Appalachian Basin: U. S. 
 
 Geol. Survey, Oil & Gas Inv. Chart OC-64. 
 
 Patchen, D. G., 1977. Subsurface stratigraphy and gas production of the Devonian 
 shales in West Virginia: MERC/CR-77/5, Morgantown, WV, 35 p. 
 
 Piotrowski, R. G., 1976a. Reef hunting in McKean County continues: Pa. Geology, 
 v. 7, no. 1, p. 2, 3. 
 
 Piotrowski, R. G., 1976b. Onondaga "reefs" - McKean County, Pennsylvania i_n 
 Lytle, W. S., Piotrowski, R. G., and Heyman, L., Oil and gas developments 
 in Pennsylvania in 1975: Pa. Geol. Survey, 4th Ser., Prog. Rept. 189, p. 29-35. 
 
39 - 
 
 Piotrowski, R. G., 1978. Devonian shale gas - new interest in an old resource: 
 
 Pa. Geology, v. 9, no. 1, p. 2-5. 
 
 Piotrowski, R. G., and Krajewski, S. A., 1977. Devonian shale research in Pennsyl 
 vania j_n Lytle, W. S., Heyman, L., Piotrowski, R. G., and Krajewski, S. A., 
 Oil and gas developments in Pennsylvania in 1976: Pa. Geol. Survey, 4th Ser. 
 Prog. Rept. 190, p. 33-42. 
 
 Piotrowski, R. G., Krajewski, S. A., and Heyman, L., 1978. Stratigraphy and gas 
 occurrence in the Devonian organic-rich shales of Pennsylvania: Proc., 1st 
 Eastern Gas Shales Symp., MERC/SP-77/5, p. 127-144. 
 
 Provo, L. J., 1976. Upper Devonian black shale - worldwide distribution and what 
 it means (Abs.) w_ Devonian Shale Production and Potential: Proc. 7th 
 Appalachian Petrol. Geol. Symp., MERC/SP-76/2, Morgantown, WV, p. 1-3. 
 
 Rickard, L. V., 1975. Correlation of the Silurian and Devonian rocks in Hew 
 York State: New York St. Mus. Sci. Ser., Map & Chart Ser. 24. 
 
 Roen, J. B., Wallace, L. G., and deWitt, W., Jr., 1978. Preliminary stratigraphic 
 cross section showing radioactive zones of the Devonian black shales in 
 eastern Ohio and west central Pennsylvania: U. S. Geol. Survey, Oil & Gas 
 Inv. Chart OC-82. 
 
 Smith, E. C., 1978. A practical approach to evaluating shale hydrocarbon poten¬ 
 tial: Preprints, 2nd Eastern Gas Shales Symp., METC/SP-78/6, vo. 2, 
 Morgantown, WV, p. 73-88. 
 
 Sutton, R. G., 1963. Correlation of Upper Devonian strata in south central New 
 York jm Shepps, V. C., ed., Symposium on Middle and Upper Devonian strati¬ 
 graphy of Pennsylvania and adjacent states: Pa. Geol. Survey, 4th Ser., 
 
 Bull. G-39, p. 87-101. 
 
 Tesmer, I. H., 1963. Geology of Chautauqua County, New York: Pt. I, Stratigraphy 
 and Paleontology (Upper Devonian): New York St. Mus. Sci. Ser., Bull. 391, 
 
 65 p. 
 
40 - 
 
 Wagner, W. R., 1976. Growth faults in Cambrian and Lower Ordovician rocks of 
 western Pennsylvania: Amer. Assoc. Petrol. Geol. Bull., v. 60, p. 414-427. 
 
 Wallace, L. G., Roen, J. B., and deWitt, W., Jr., 1977. Preliminary stratigraphic 
 cross section showing radioactive zones in the Devonian black shales in the 
 western part of the Appalachian Basin: U. S. Geol. Survey, Oil & Gas Inv. 
 Chart OC-82. 
 
 Woodward, H. P., 1961. Preliminary subsurface study of southeastern Appalachian 
 Interior Plateau: Amer. Assoc. Petrol. Geol. Bull., v. 45, p. 1634-1655. 
 
 Wright, N. A., 1973. Subsurface Tully Limestone, New York and northern Pennsyl¬ 
 vania: New York St. Mus. Sci. Ser., Map & Chart Ser. 14. 
 
 ☆ U.S. GOVERNMENT PRINTING OFFICE: 1980 0— 311-344/48 
 

 
 
 
 
 
 
 ' 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 

Well showing thickness of interval from top of Dev on ion to baseofMorcellus 
 
Plate I 
 
 Scale 1 : 1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J A HARPER 
 
 
 
 ISOPACH OF 
 
 INTERVAL 
 
 FROM 
 
 TOP 
 
 
 OF DEVONIAN 
 
 TO BASE OF 
 
 MARCELLUS 
 
 ^500^ 
 
 Contour Intervol = 500 feet 
 
 
 
 
 Thick 
 
 ness of intervol from top o 
 
 f Devonion to bose of Morcellus 
 
 
 / 
 
 r 50 0" 
 
 1 n fer 
 
 red thickness of intervol f 
 
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 us 
 
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 see Geologic Mop of 
 
 Pennsylvania, I960) 
 
 
 
 o* 
 
 Well 
 
 identification number 
 
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 for 
 
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 or 
 
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 UNIVERSITY OF ILLINOIS 
 
Plate 2 
 
 Scale 1 : 1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 B.G. PIOTROWSKI AND J.A.HARPER 
 
 TOTAL NET FEET OF RADIOACTIVE 
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 UNIVERSITY OF HTT 
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Plate 3 
 
 Scale 1:1,000.000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A.HARPER 
 
 ISOPACH OF THE HAMILTON GROUP 
 
 Contour intervol = 50 feet 
 50 y Thickness of totol Homilton Group 
 
 
 Generalized boundory of Mississippian (M ) - Devon ion (D) outcrop (for de 
 tail, see Geologic Mop of Pennsylvania, I960) 
 
 Well identification number (see Penn. Geol. Survey Open File Rept. 1,1970) 
 for wells penetrating the Tally Limestone or deeper 
 
 Well showing totol thickness of Homilton Group 
 Well with Fault in Hamilton Group 
 
 UNIVERSITY OF TIT? NOT!? 
 GEOLOGY LIBRARY 
 
 638 # 
 
 M 
 
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 3 / 3 ? 
 
Plate 4 
 
 Scale 1 : 1,000,000 
 
 140 K ILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI ANO J A HARPER 
 
 NET FEET OF RADIOACTIVE SHALE 
 
 IN 
 
 THE HAMILTON GROUP 
 (MARCELLUS FACIES) 
 
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 f Z 5 NeI ,eet 'Odiooctive shole in the Homilton Group 
 
 V Gtnf ' 0lizfd b0und0rv ° f Mississippi (MJ-Devonion (D) outcrop (to, de 
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 for wells penetroting the Tully Li 
 
 ol. Survey Open File Re pt. 1,1970) 
 
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Plate 5 
 
 Scale 1:1,000,000 
 
 140 K ILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A.HARPER 
 
 Contour interval = 500 feet 
 ^-500 Structure on top ofOnondogo Group 
 
 Generalized boundary of M , ss i ss i p p ia n ( M ) - De v o n i a n ID) outcrop (for de- 
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 40 
 
 60 
 
 '20 _140 KILOMETERS 
 
 ISOPACH OF TULLY LIMESTONE 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J A HARPER 
 
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 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R t PIOTROWSKI ANO J.A.HARPER 
 
 
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 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A.HARPER 
 
 ISOPACH OF TOTAL UPPER DEVONIAN SHALE 
 
 Contour infervol = 500feet 
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 M^/ Generolized boundory of Mississippi on (M)- Devonian (D) outcrop (for de 
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 Well showing Totol Upper Devonion Shole 
 
 Zsoo Well showing minimum thickness of Totol Upper Devonion Shole 
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 UNIVERSITY OF ILLINOIS' 
 
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 40 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
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 BUREAU OF TOPOSRAPHIC ANO 6E0L06IC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPAREO UNDER CONTRACT TO 
 BEPARTMINT OF ENERGY BY 
 R & PIOTROWSKI ANO J A HARPER 
 
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 50^ Thickness of Genesee Formotion 
 
 M/ Generalized boundary of M is si, s i p p ion (M)- Devonian (D) outcrop (for de- 
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 UNIVERSITY OF ILLINOIS 
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 ISOPACH OF BURKET-GENESEO-RENWICK 
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 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
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 THE GENESEE FORMATION 
 (BURKET-GENESEO- RENWICK FACIES) 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J A HARPER 
 
 
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 toil, 
 
 see Geologic Mop of Pennsylvoni 
 
 o, I96 0) 
 
 
 
 ° 9 
 
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 ide nti f i co ti o n number (see Penn. 
 
 Geol. 
 
 S u r 
 
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 le Rept 
 
 
 for 
 
 wells pe n e l r o l in g ihe Tully Limestone 
 
 or 
 
 deeper 
 
 
 O 12 
 
 Wei 1 
 
 showing net feet of rodiooctive 
 
 shole 
 
 in 
 
 Genesee Formolion 
 
 R5ITY OF ILLINOIS 
 
 : lODADV 
 
Plate 13 
 
 Deyi./' 
 
 Hoh^rt 
 
 
 / 
 
 
 
 
 
 \ 
 
 
 _J 
 
 
 
 / 
 
 
 Sc»l« 1 : 1,000,000 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI ANO J.A.HARPER 
 
 Contour interval = 50 feet 
 ^50^ Net thickness ofthe Sonyeo Formotion 
 
 Generalized boundary of Mississippi (M ) -Devonian (0) oulcrop (for de- 
 ' 011 • see Geologic Map of Pennsylvania, I960) 
 
 Well idenlificanon number (see Penn. Seal. Survey Open File Rept. I,.1970) 
 
 for wells pene froting the Tully Limestone o, deepe 
 WeM showing thickness of the Sonyea Formotion 
 * WeM wllh *oult in Sonyeo Formotion 
 L,mi ' °f identifiable Sonyeo Formation 
 
 Diversity of Illinois 
 
Plote 14 
 
 Regionol studies indicate the Sonyeo 
 Formation obsent in this oreo. 
 
 Scale 1:1,000.000 
 40 
 
 60 
 
 140 K ILOMETERS 
 
 NET FEET OF RADIOACTIVE SHALE 
 
 IN 
 
 SONYEA FORMATION 
 (MIDDLESEX FACIES) 
 
 Contour intervol = 25 feet 
 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R.G. PIOTROWSKI ANO J A HARPER 
 
 r 
 
 25 Net thickness of radiooclive shale in Sonyea Formation 
 
 M/’ Ge ner aliz ed boundary of M is s iss ip p io n ( M ) — Devonian (D) oulcrop (for de 
 
 toil, see Geologic Mop of Pe nns y Ivoni o, I960) 
 
 Well identification number (see Penn. Geol. Survey Open Fi le Re pi. 1,197 0) 
 for wells penetrating the Tully Limestone o, deeper 
 
 Well showing net feet of radioactive shale in Sonyeo Formation 
 
 UNIVERSITY OF ILLINOIS 
 
 GF/Tf I IDOAnw 
 
1 
 
Plate 15 
 
 Scale 1 : 1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A.HARPER 
 
 STRUCTURE ON BASE OF MIDDLESEX 
 RADIOACTIVE SHALE FACIES 
 
 Contour interval = 500 feet 
 ^ 50 ° X structure on bose of Sonyeo Formotion 
 
 My Generalized boundary of M i s si ss I p p io n ( M ) -Devonian (D) outcrop (for de - 
 loll, see Geologic Mop of Pe nnsy I vo n i o , I960) 
 
 o» Well identification number (see Penn. Geol. Survey Open File Rept. 1,1970) 
 for wells penetroting the T u 11 y Limestone or deeper 
 
 ? " J< Well showing depth below sea level to bose of Sonyeo Formotion 
 
 y Limit of Identifiable Sonyeo Formation 
 ^ i"ftolL recognized within the Sonyeo Formation 
 r * Well with fault in Middlesex shole focies 
 
 
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Plote 16 
 
 Scale 1 : 1,000,000 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R.G. PIOTBOWSKI AND J.A.HARPER 
 
 
 Contour intervol = 50 feet 
 Thickness of West Foils Formation 
 
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 Well identification number ( 
 
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Plate 17 
 
 Scale 1 : 1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF RADIOACTIVE SHALE 
 
 IN 
 
 THE WEST FALLS FORMATION 
 (RHINESTREET FACIES) 
 
 Contour intervol s 25 feet 
 
 ,/ 
 
 /- 25 Net feet rodiooctive shole in the West Foils Formation 
 
 M/ G e n e r o I i z e d boundary o, Mltsissippian (M)“ Devonian <D> outcr.p ( , or dt 
 
 ' “ e Geologic Mop of Pennsylvania, I960 ) 
 
 015 — <’«• P-n. Geo,. Survey Open File Rept. , l97( 
 
 for .ells penetrating the Tally Limestone or deeper 
 
 °— . dentlficotion number (see Penn. Geol. Survey Open File Slept | 197 
 
 well, ending before penetration of the Tull, Limestone 
 
 well showing net feet 0 . radioactive shole 
 
 in West Foils Formation 
 
 Well showing minimum net feel of rodiooc ,,e shole 
 
 in West Foils Formotio 
 
Q 
 
Plate 18 
 
 Scale 1:1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A.HARPER 
 
 
 
 STRUCTURE ON 
 
 BASE OF RHINESTREET 
 
 
 
 R A D10 ACT 
 
 1 VE 
 
 SHALE FACIES 
 
 
 Cont 
 
 our intervol = 500 feet 
 
 
 
 500^” 
 
 Structure on bose of Rhinestree 
 
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 V 
 
 Gene 
 
 rolized boundory of M 
 
 issis s 
 
 ppion (M ) - Devonion (D) outcrop ( for de- 
 
 ' D 
 
 toi l t 
 
 see Geologic Mop of 
 
 Penns 
 
 l \v onio, I960) 
 
 
 Well 
 
 idenlificotion number 
 
 ( see 
 
 Penn. Geol. Survey Open File Rept. 1, 1970) 
 
 
 for 
 
 well s pene t roti n g the 
 
 Tull y 
 
 Limestone or deeper 
 
 
 Well 
 
 showing depth below seo 
 
 level 
 
 o bose of Rhinestreet rodiooctive shole focies 
 
 °-rsi3 
 
 (or 
 
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 s' 
 
 / 
 
 L i m 
 
 it of Rhi nestreet rodiooctiv 
 
 shole 
 
 focies (or morker) 
 
 F 
 
 Fou 
 
 t 
 
 
 
 UNIVERSITY OF ILLINOIS, 
 
 GEOLOGY IBRARY 
 
Plate 19 
 
 Scale 1 : 1,000 ,000 
 
 140 K I LOME T ERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A.HARPER 
 
 . 25-'' 
 
 Conlour i n I e f v o I = 25 feet 
 Thickness of Jovo Formofion 
 
 V. 
 
 Generalized boundary of M is s is s . ppi a n ( M ) - De , o n ia n ( D ) 
 'oil, see Geolog.c Map of Pennsyl 
 We II id entificotion 
 
 outcrop (for de - 
 
 sylvomo, i960) 
 
 number (see Penn. Geol. Survey Open File Rept. I, 1970) 
 for wells penetrating the Tolly Limestone or deeper 
 
 Well idenlificotion number (see Penn. Geol. Survey Open File 
 'O' ” ellS endi " 9 be,ore Penetrotion of Ihe Tully Limestone 
 
 Rept. I, 1970) 
 
 Well showing thickness of Jovo Formoti 
 Limit of Pipe Creek rodioocti 
 
 ve shole focies 
 
 UNIVERSITY OF ILLINOIS 
 
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Plate 20 
 
 Scale 1 : 1,000,000 
 
 1 ? 0 _140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J A. HARPER 
 
 STRUCTURE ON BASE OF PIPE CREEK 
 RADIOACTIVE SHALE FACIES 
 
 500- 
 
 Contour in te r vo I = 500f l. 
 
 Structure contour onthe bose of The Pipe Creek rodiooclive shole focies 
 
 G e nerol I zed boundory o, M i s si s s i pp i a n { M ) — Devonion (0) outcrop (, or 
 tail, see Geologic Mop of Pen n sy I v on io, I 960 ) 
 
 Well Identified. ion number (see Penn. Geol, Survey Open F, le Rept. I, l< 
 
 for wells penetrating the Tally Limestone or deeper 
 
 Well identification number (,ee Penn. Geol Survey Open File Rept. I l 
 
 for wells ending before penetrotion of the Tully Limestone 
 
 Well showing depth below seo level of bose of p,pe Creek rod,ooctive shole focies 
 
 5h0 " in 9 height above seo level of bose of Pipe Creek radioactive shole focies 
 - Limit of the Pipe Creek rodioocotve shole focies 
 
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Plate 21 
 
 Scale 1:1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF RADIOACTIVE SHALE 
 
 IN 
 
 THE CANADAWAY GROUP 
 (DUNKIRK FACIES) 
 
 Contour intervol = 25 feet 
 ^ Net feet rodiooctive shole in the Westfalls Formotion 
 
 Generalized boundory of M i ssiss ippio n ( M ) - Devonion ( D) outcrop (for de- 
 * toil, see Geologic Mop of Pe nnsyl vo n io, I960) 
 
 Well Identification number (see Penn. Geol. Survey Open File Rept. 1, 1970) 
 for wells penetroting the Tally Limestone ordeeper 
 
 Well identification number (see Penn. Geol. Survey Open File Rept. I, 1970) 
 for wells ending before penelrotion of the Tully Limestone 
 
 ° 9t Well showing net feet of rodiooctive shale in Westfalls Formotion 
 
 UNIVERSITY OF ILLINOIS 
 
 GEOLOGY LIBRARY 
 
 Milo n •? *58? 
 
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Plote 22 
 
 Scale 1:1.000,000 
 
 1 1 Q _140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R.G. PIOTROWSKI AND J.A.HARPER 
 
 STRUCTURE ON BASE OF DUNKIRK 
 RADIOACTIVE SHALE FACIES 
 
 Contour intervol = SOOfeet 
 
 500 Structure contour on the bo s e of th e Dunkirk rodiooctive shole focies 
 
 I J Generalized boundory of M is s i ss i pp i o n (M)- Devonian (D) outcrop ( for de- 
 
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 Well i de nt i f i cot ion number (see Penn. Geol. Survey Open File R e p t. I, 1970) 
 o 9 
 
 for wells penetroting the Tully Limesione or deeper 
 
 o2 
 
 Well identification number (see Penn. Geol Survey Open File Repi. I, 1970) 
 for wells ending before peneirotion of the Tully Limestone 
 
 Q.I234 Well showing depth below seo level of bose of Dunkirk rodiooctive shole focies 
 °204 well Showing heigh t obove se o leve I of bose o f Dunkirk rodiooctive shole focies 
 
 .—-Limit of I he D un kirk rodiooctive shole focies 
 
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 Scale 1:1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R.G. PIOTROWSKI AND J. A.HARPER 
 
 ISOPACH OF TOTAL SAND 
 (Zones D, B, and Bo or Zone D-B-Bo) 
 
 Contour intervol =500 feet 
 
 
 ,500^ Thickness of totol Upper Devonion sand, dashed where uncertoin 
 
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 Geol. 
 
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 fo r 
 
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 UNIVERSITY OF ILLINOIS 
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 Scale 1:1,000,000 
 
 MO KILOMETERS 
 
 NET FEET OF SAND 
 in COMBINED ZONES D.B.and Bo 
 
 r 
 
 M 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A.HARPER 
 
 Contour intervol =100 feel 
 
 100-^ Net feel of sond in combined Zones D,B,ond Bo, doshed where uncertoin 
 / Generolized boundory of Mississippion ( M ) - Devon ion (D) oulcro p (for de 
 ^ toil, see Geologic Mop of Pennsylvonio, I960) 
 j Well i den t i f i co t i o n number (see Penn Geol Survey Open file Rept. I, 1970) 
 
 for wells penetroling the Tully Limestone or deeper 
 
 - Well identificotion number (see Penn. Geol Survey Open File Rept I, 1970) 
 
 for wells ending before penetrotion of the Tully Limestone 
 Qrj Well showing net feet of sond mcombined Zones D, B ,ond Bo 
 0 ^ Well showing minimum net feet ofsond combined Zones 0, B,ond Bo 
 
 UNIVERSITY OF ILLINOIS' 
 
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 Scale 1 :1,000,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R.G. PIOTROWSKI AND J.A.HARPER 
 
 -500-^ 
 
 Contour Interval = 500 feet 
 Thickness of Zone Bo sand 
 
 Limit of Zone Bo 
 
 Generalized boun dory of Mississippi on (M) — Devonian (D) outcrop (for de 
 tail, see Geologic Map of Pennsylvania, I960) 
 
 Well identification number (see Penn. Geol. Survey Open File Rept. I, 1970) 
 for wells penetrating the Tull y Limestone or deeper 
 
 v f/*3 
 
 2///J 
 
 Well identification number (see Penn Geol. Survey Open File Rept 1,1970) 
 for wells ending before penetrotion of the Tully Limestone 
 Well showing thickness of Zone Bo sand 
 Well showing minimum thickness of Zone Bo sand 
 
 UiMIVL . . ; ul.1 
 
 geology 
 
Scale 1 : 1,000 ,000 
 
 140 K I LOME T ERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J. A HARPER 
 
 
 
 NET FEET OF SAND 
 
 IN ZONE Bo 
 
 
 
 
 Con to 
 
 ur in tervo 1 = 25 feet 
 
 
 
 
 
 
 25—'' 
 
 Net f 
 
 ee t of sond Zone Bo 
 
 
 
 
 
 
 
 Li mi t 
 
 of Z one B o 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 m y 
 
 6e n e 
 
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 ( M ) - Oe vo n 
 
 on (0 ) ou 
 
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 for de- 
 
 / 3 
 
 toil, 
 
 see Geologic Map of 
 
 Pe n nsy Iv o n io 
 
 , I960) 
 
 
 
 
 o 5 
 
 Wei 1 
 
 i dent Ificotion num ber 
 
 (see Penn. 
 
 Geol. Survey 
 
 Open File 
 
 Re pt. 
 
 1, 1970) 
 
 
 fo r 
 
 wells penetrating the 
 
 Tu 11 y Lime 
 
 stone or de 
 
 eper 
 
 
 
 O- 
 
 Well 
 
 identification number 
 
 (see Penn. 
 
 Geol. Survey 
 
 Open Fi le 
 
 R ept 
 
 1, 1970) 
 
 
 for 
 
 wells ending before 
 
 enetra tion 
 
 f the TuII y 
 
 Limesto ne 
 
 
 
 ©74- 
 
 Well 
 
 showing net feet ofsond 
 
 n Zone Bo 
 
 
 
 
 
 O 72 
 
 Wei 1 
 
 showing minimum net feet 
 
 of s o nd in Zo 
 
 e Bo 
 
 
 
 
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Scale 1 :1,000,000 
 
 i0 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A HARPER 
 
 
 
 ISOPACH OF T 
 
 HE 
 
 ZONE 
 
 B 
 
 SANDS 
 
 
 
 Conio 
 
 ur in ter vo 1 s 500 fe et 
 
 
 
 
 
 
 
 ^.500-^ 
 
 Thick 
 
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 see Geologic Mop of Penns 
 
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 Well 
 
 identificotion number (see 
 
 Penn. 
 
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 Rept. 1, 1970) 
 
 
 for 
 
 wells penetroting The Tolly 
 
 L i m 
 
 estone or 
 
 de 
 
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 o* 
 
 Wei 1 
 
 identificotion number (see 
 
 Penn 
 
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 Rapt 1, 1970) 
 
 
 for 
 
 wells ending before penetrotio 
 
 n of 1 
 
 he Tully Limesto 
 
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 Well 
 
 showing thickness of Zone B so 
 
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 Wei 
 
 showing minimum thickness 
 
 of Zo 
 
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 UNIVERSITY -f 
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Scale 1:1,000,000 
 <0 
 
 60 
 
 60 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW. STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J A HARPER 
 
 NET FEET OF SAND IN ZONE B 
 
 Contour iniervol = 50 feet 
 
 ^,50—^ Net feet of sand in Zone B 
 
 
 Li mi 
 
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 see Geologic 
 
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 Pe n nsy Iv 0 n 10 , I960) 
 
 
 
 o* 
 
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 i den tif i cot ion 
 
 n u m ber 
 
 (see Penn. Geol. Survey Open File 
 
 R e p t 
 
 l, 1970) 
 
 
 for 
 
 wells penetroting the 
 
 Tully Limestone or, deeper 
 
 
 
 0 - 
 
 Well 
 
 identification 
 
 number 
 
 Isee Penn Geol. Survey Open File 
 
 R e p t 
 
 1,1970) 
 
 
 for 
 
 wells ending 
 
 before peneirotion of the Tully Limestone 
 
 
 
 o t3 4 Well showing nei feet of sona in Zone B 
 
 Ogr Well showing minimum net feet of sond in Zone B 
 
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 Scale 1:1,000,000 
 
 120 _140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF SAND IN ZONE Bl 
 
 
 Contour mtervol : 50 feet 
 
 
 
 ^-50 ^ 
 
 Net 
 
 feet of so nd in Zone 8 l 
 
 
 
 
 Limit 
 
 of Zone Bl 
 
 
 
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 see Geologic Mop of Pennsylvomo, i960) 
 
 
 
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 Re p t 
 
 1, 1970) 
 
 
 for 
 
 wells penetroting the Tully Limestone or deeper 
 
 
 
 o! 
 
 Well 
 
 id en tif icotion number (see Penn Geol Survey Open File 
 
 R e p t 
 
 1, 19 70) 
 
 
 for 
 
 wells ending before penetrotion of the Tully Limestone 
 
 
 
 °« 
 
 Wei 1 
 
 showing net feet of sond in Zone Bl 
 
 
 
 
 Well 
 
 Showing minimum net feet of sond in Zone Bl 
 
 
 
 UNIVERSITY OK ILLINOIS 
 GEOLOGY LIBRARY 
 
Scale 1:1,000.000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI ANO J A HARPER 
 
 NET FEET OF SAND IN ZONE B2 
 
 Contour interval = 25 feet 
 Net feet of sand in Zone B2 
 Limi t of Zone B2 
 
 Generalized boundary of Ml s s is si p p i on (M) - Devonion (D) outcrop ( for de¬ 
 
 tail, see Geologic Mop of Pe n n sy I ua ma , I960) 
 
 Well Identification number (see Penn. Geol. Survey Open File Rept- 1,1970) 
 
 for wells penetrating the Tully Limestone or deeper 
 
 Well Identification number (see Penn. Geol. Survey Open File Rept. 1,1970) 
 for wells ending before penetration of the Tully Limestone 
 
 Well showing net feet of sand in Zone B2 
 
 Well showing minimum net feet of sand in Zone 82 
 
 UNIVERSITY OF ILLINOIS 
 GEOLOGY LIBRARY 
 
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 Scale 1 : 1,000.000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF SAND IN ZONE B4 
 
 Contour i n ter v o | : 50feet 
 
 Net fee t of sond m Zone B 4 
 Limit of Zone B4 
 
 M ( 
 
 Ge n ero l ized bounder, of M i s sis s i p p i a n (M) - Devonion ID) outcrop (,or de 
 toil, see Geologic Mop of Pe n n Sy I vo n. o , i960) 
 
 i denti 
 
 if i C 0 t ion number 
 
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 Penn 
 
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 Open File 
 
 Re p t 
 
 1, 1970) 
 
 wells 
 
 pe n e t 
 
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 Tull 
 
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 identi 
 
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 ( see 
 
 Penn 
 
 Ge o l Survey 
 
 Open File 
 
 R e p t 
 
 I, 1970) 
 
 wells 
 
 e n d i ng 
 
 before peneft 
 
 • 0 ti o n 
 
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 Zone 
 
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 show 
 
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 feel 
 
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 Scale 1 : 1.000,000 
 
 UO KILOMETERS 
 
 THE PENNSYLVANIA OEPT. OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF SAND IN ZONE D 
 
 
 Cont 0 
 
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 Pennsylvania, I960) 
 
 
 
 
 
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 Well 
 
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 number 
 
 (see Penn. Geol Survey 
 
 Open File 
 
 Re pt. 
 
 1, 1970) 
 
 
 
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 Tully Limestone or de 
 
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 6 ? 32 < 31 
 
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 Well 
 
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 1, 1970) 
 
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 wells 
 
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 feet of sand in Zone D 
 
 
 
 
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 UNIVERSITY OF ILL'INP 1 '? 
 
 Gcof.onv 
 
Scale 1 : 1,000 ,000 
 
 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF SAND IN ZONE D1 
 
 
 Conte 
 
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 25 feet 
 
 
 
 
 
 
 
 
 Net 
 
 feet of sand in 
 
 Zone D 1 
 
 
 
 
 
 
 
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 see Geologic 
 
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 Re pt. 
 
 1, 1970) 
 
 
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 identification 
 
 number 
 
 ( see Penn. 
 
 Geol. Sur 
 
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 Open File 
 
 R e pt. 
 
 1, 1970) 
 
 
 for 
 
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 before 
 
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 140 KILOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J.A HARPER 
 
 NET FEET OF SAND IN ZONE D2 
 
 
 Contour miervo I : 25feet 
 
 
 
 Net feet of sond in Zone 02 
 
 
 
 Limit of Zone 02 
 
 
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 Ge n e ro 1 ized boundory of Missis sippion (M)— Devonion 10) outcrop 
 
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 Well identif icotion number Isee Penn Geol. Survey Open File Rept 
 for wells penetroting the Tully Limestone or deeper 
 
 1, 1970) 
 
 o- 
 
 Well i d e n 11 f i c o f i o n number (see Penn Geol Survey Open File Rept 
 for wells ending before penetro lion of the Tully Limestone 
 
 1, 1970) 
 
 
 Well showing net feet of sond in Zone 02 
 
 
 ° ff 
 
 Well showing minimum net feet of sond in Zone 02 
 
 
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Plate 38 
 
 Scale 1 : 1,000,000 
 
 40 K UOMETERS 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J A.HARPER 
 
 
 
 
 NET 
 
 FEET 
 
 OF SAND IN ZONE 
 
 D3 
 
 
 
 Con to 
 
 u r i 
 
 ntervol = 
 
 25 feel 
 
 
 
 
 
 
 y-Zb-S' Net 
 
 feet 
 
 f so n d in 
 
 Zone 03 
 
 
 
 
 
 
 
 Limit 
 
 of Zor 
 
 e D3 
 
 
 
 
 
 
 
 M / 
 
 Gene 
 
 olized 
 
 boun do 
 
 ry of M 
 
 1 S S IS S i PP 10 
 
 ( M ) - Devon 
 
 o n ( 
 
 0) outcrop 
 
 for de- 
 
 r D 
 
 1 o i 1, 
 
 see 
 
 G e o l o g ic 
 
 Mop of 
 
 Pennsylvon 
 
 o, I960) 
 
 
 
 
 o 5 
 
 Well 
 
 i d e n t 
 
 f i co ♦ ion 
 
 number 
 
 (see Pen n 
 
 Geol Survey 
 
 0 per 
 
 File Re pt 
 
 1, 1970) 
 
 
 for 
 
 wells 
 
 pe n e t r c 
 
 ting the 
 
 T u 1 1 y L i m 
 
 estone or de 
 
 e p e r 
 
 
 
 
 Well 
 
 idem 
 
 i f i co ti o n 
 
 number 
 
 (see Penn 
 
 Geol Survey 
 
 Op-en 
 
 File R e p t. 
 
 1, 1970) 
 
 
 for 
 
 wells 
 
 ending 
 
 before 
 
 )ene t r o tion 
 
 of th e Tu lly 
 
 Lime 
 
 stone 
 
 
 
 Wei 1 
 
 show 
 
 mg net f 
 
 e e t of so 
 
 d i n Z o n e 
 
 D 3 
 
 
 
 
 
 Well 
 
 show 
 
 i n g mm 
 
 mum net 
 
 feet of so 
 
 d in Zone 0 3 
 
 
 
 
 6 3 H 
 
 ■ m 
 
 Si/cur 
 
 .Py 
 
 3 S/ 3 ? 
 
 L ;; ivtlRSITY OF ILLINOIS 
 geology library 
 
 M> /3 
 
Plote 39 
 
 Scale 1 : 1,000.000 
 
 |40 KILOMETERS 
 
 ^ 50 ' 
 
 THE PENNSYLVANIA DEPT OF ENVIRONMENTAL 
 
 RESOURCES 
 
 BUREAU OF TOPOGRAPHIC AND GEOLOGIC 
 SURVEY 
 
 ARTHUR A. SOCOLOW, STATE GEOLOGIST 
 PREPARED UNDER CONTRACT TO 
 DEPARTMENT OF ENERGY BY 
 R G. PIOTROWSKI AND J A HARPER 
 
 Contour interval = 50feet 
 
 / o 
 
 Thickness of Riceville Shale 
 Limit of Zone D sand 
 
 Generalized boundary of Missis s ippi on (M)— Devonian (D) outcrop ( for de¬ 
 
 tail, see Geologic Map of Pennsylvania, I960) 
 
 Well identification number (see Penn Geol. Survey Open File Rept. I, 1970) 
 for wells penetrating the Tully Limestone or deeper 
 
 Well identification number (see Penn Geol Survey Open File Rept I, 1970) 
 for wells ending before penetration of the Tully Limestone 
 
 Well showing thickness of Riceville Shale 
 
 Well showing minimum thickness of Riceville Shole 
 
 UNIVERSITY OF ILLINOIS 
 GEOLOGY LIBRARY 
 
 MAR C 2 1982 
 
 '' 1 1 
 
 , 8 
 si/ur NO 43 
 • py 
 
 3 ?/ 39