A FIELD AND PETROGRAPHIC STUDY OF THE SANDSTONES AND CONGLOMERATES OF THE PORCUPINE MOUNTAINS, ONTONAGON COUNTY, MICHIGAN by HATEM HUSSEIN EL-KHALIDI A THESIS Submitted to the School of Graduate Studies of Michigan State College of Agriculture and Applied Science in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Geology and Geography 1950 ProQuest Number: 10008739 Alt rights reserved INFORMATION TO ALL USERS The quality o f this reproduction is dependent upon the quality of the copy submitted. In the unlikely event that the author did not send a complete manuscript and there are missing pages, these will be noted. Also, if material had to be removed, a note will indicate the deletion. uest. ProQuest 10008739 Published by ProQuest LLC (2016). Copyright of the Dissertation is held by the Author. All rights reserved. This work is protected against unauthorized copying under Title 17, United States Code Microform Edition © ProQuest LLC. ProQuest LLC. 789 East Eisenhower Parkway P.O. Box 1346 Ann Arbor, Ml 4 8 1 0 6 - 1346 ACKNOWLEDGMENTS The writer wishes to express his gratitude to Dr, W.A. Kelly for outlining the field procedure of this study, sup­ plying aerial photographs, hase and topographic maps, and giving valuable suggestions for the improvement of this paper. The writer wishes to express his sincerest thanks to Dr, B,T. Sandefur who gave freely of his time and effort in supervising the laboratory procedure, and for his invaluable help in the writing of this paper. To Drs. S.G. Bergquist and J. Trow, the writer wishes to convey his deep appreciation and thanks for their help in reading and editing this paper, and for their valuable sug­ gestions on the style. The field work of this paper would not have been possible without the active help of Mr, Joseph Elliot to whom the writer is very much indebted. TABLE OF CONTENTS Page I N T R O D U C T I O N .............................. 1. 2. 3. 4. L o c a t i o n ............................ General Topography ........ . . . . General Geology..................... Purpose of Study . . . . . ......... 1 1 1 2 14 P R O C E D U R E ................................ 18 1. Field Procedure. ............. 2. Laboratory Procedure ............... 18 18 DESCRIPTION OF SECTIONS................... 21 1. 2. 3. 4. 5. 6. 7. Section I ......................... Section II . . ..................... Section I I I ................ Section I V ......................... Section V ......................... Section V I ........... General Statement................... 21 24 27 33 36 41 43 MINERALOGY AND P E T R O G R A P H Y ............... 49 1. The S a n d s t o n e s ..................... 2. The Igneous Pebbles................. 3. General Statement............ 49 57 60 CORRELATIONS . .......................... 63 C O N C L U S I O N ................................ 66 A P P E N D I X .................................. 70 DESCRIPTIONS OF SAMPLES OF THE SECTIONS 1. 2. 3. 4. 5. 6. Section I ......................... 70 Section I I . . ................... 74 Section I I I .................. 78 Section I V ......................... 87 Section V .................... 90 Section VI ...................104 BIBLIOGRAPHY 109 LIST OF ILLUSTRATIONS Page 1 2 3 4 5 6 17 17 68 68 69 69 LIST OF MAPS Following page Map 1 2 1 110 LIST OF PLATES Following page Plal 1 , 110 IV 1 INTRODUCTION 1# Location The Porcupine Mountains area is located in Ontonagon and Gogebic Counties, between the Iron and the Presque Isle Rivers in the Upper Peninsula of Michigan (Map 1). The area is a State park, which is easily reached from Silver City, Michigan, on State Highway M-107. 2. General Topography The Porcupine Mountains rise from the shore of Lake Superior in T. 51 N., Rs. 42, 43, and 44 W, as roughly con­ centric ridges parallel to the shore line* The first ridge, rising from the shore of Lake Superior, reaches a height of 850 to 900 feet above the lake level, within a mile and a half to the south (Plate 1). It then descends abruptly 400 feet into the valley of the Carp Ri­ ver. This river follows a very irregular course from its headwaters to the southeast, empties into the Lake of the Clouds, and then proceeds in a southwesterly direction and empties into Lake Superior at a location in the northeast corner of Gogebic County. Beyond the Carp River to the south, there is a steep escarpment leading up to an eroded plateau and the valley of the Little Carp River. Knobs and ridges occur, but these are not as extensive or as steep as the first ridge. In this area the highest elevations of the Porcupine Mountains occur. The highest point, as listed by the Michigan Department of Conservation, is Government Peak. It is 2,023 feet above sea MICHIGAN ,HTON Lake PRE-CAMBR/AJV sup £ f\(j DOMINION OF CANADA O N D '^C huronlA T e ^ j IACKINAC DICI "SALJNA O^JVACKINAC EMMET /N CHEBOYGAN P R E S Q U E I5 L I KEWEENAWAN SERIES ALL i SCODA ALCONA I EN ZI E M IC R IG A N .CO W£ X FORI I AC !a DWIN .ARE MASON BAY BEDS" ISABELLA NEWAYI TUSl S A G IN A V ATIXJT SAGINAW MUSKZGON "R E D It t a w a ^ C LINTOI 'B E D S / T)RY ALLEGA| Ia t o n OAKLAND I NGHAM S A & /N A W SDUNDEE KALAMAZO CANADA 'D E T R O IT R l/S E R BRA NC H C ASS JOSEPH MAP J- SHOWING LOCATION OF AREA STUDIED AND THE A R EA L LENAWJ r' S Y LV A N /A 1 * LAKE 'BASS G L A N D 'V ERIE D IS T R IB U T IO N OF THE KEWEENAWAN SERIES 2 level, or 1,421 feet above the level of Lake Superior; but as far back as 1908, A.C. Lane and others have indicated that this figure is too high* Lane believed it to be closer to 1,860 feet above sea level* More recent and accurate meas­ urements based on field work and study of aerial photographs by Dr* W.A* Kelly of the Department of Geology, Michigan State College, show that another peak to the southeast of Government Peak is the highest* Dr. Kelly assigns an eleva­ tion of 1,900 to 1,950 feet above sea level to this peak. The Little Carp River empties into Mirror Lake in the heart of the Porcupine Mountains, then into Lily Pond to the southwest, and finally into Lake Superior at a location approx­ imately one mile southwest of the mouth of the Carp River* Rainfall in the Porcupine Mountains is relatively heavy, and the elimination of the meteoric water by drainage and evaporation is small; thus, large sw'amp areas are present. Some areas around the valley of the Carp River are swamps. Others are located about a mile southeast of Government Peak. 3. General Geology The rocks that outcrop in the Porcupine Mountains belong to the series known as the Keweenawan. A description of the general character of the Keweenawan rocks is essential to the understanding of the rocks of the Porcupine Mountains, because of the very close relationship between them and the other Keweenawan rocks that outcrop elsewhere, especially in the Keweenaw Peninsula and along the Black River to the southwest of the Porcupine Mountains. 3 Distribution of the Keweenawan Rocks: The area in which these rocks are exposed lies in the southern segment of the pre-Gambrian shield of North America and forms a part of the Lake Superior basin* Along the south shore of the lake, the area extends from Keweenaw Point in Michigan southwestward through northern Wisconsin and into Minnesota. The Keweenawan rocks border the north shore of Lake Superior in Minnesota to the Canadian boundary, crop out in Isle Royale, and in Canada appear in the Black Bay and Thunder Bay dis­ tricts, and extend to the area around Lake Nippigon. Character of the Rocks: The Keweenawan series are com­ prised of coarse clastic sediments together with intrusive and extrusive igneous rocks. Both the base and the upper part of the series are composed of sediments. The basal sed­ iments, with a maximum thickness of 1,500 feet, are overlain by great thicknesses of basaltic lava flows interspersed with relatively thin sediments and acidic lava flows. The upper part of the Keweenawan series is composed wholly of thick conglomerate overlain by thin shale -which, in turn, is overlain by thick sandstone. Age of the Rocks: In the Gogebic Iron Range of Michi­ gan, the Keweenawan is underlain by Penokee-Gogebic iron series which are upper-Huronian in age. In the Black River section there is a space of nearly half a mile between the lowest exposures of the Keweenawan, and the highest exposures of the Penokee-Gogebic; thus, no direct evidence of an 4 unconformity exists. Irving* suggested that a disconformity * Irving, R .D., "The Copper Bearing Rocks of Lake Superior", United States Geological Survey, Monograph 5 , p. 24 (1883). occurs between the Keweenawan and Huronian. A complete dis­ cussion of a possible conformity or unconformity between the Keweenawan and the Huronian is given by Irving and Van Hise in the United States Geological Survey, Monograph 19, on the Penokee-Gogebic Range. Overlying the upper Keweenawan without apparent uncon­ formity or abrupt change in character, is the Lake Superior sandstone which is considered by the United States Geologi­ cal Survey to be upper-Cambrian in age. The United States Geological Survey groups the Keweenaw­ an as upper-Proterozoic, of pre-Gambrian age. disagree with this classification. Some geologists A.C. Lane* argues that * Lane, A.C., "The Keweenawan Series of Michigan," Michigan Geological Survey, Publication 6 (Geol. Series 4), 2 vol., 983 pp. (1911). since the apparently major unconformity lies below the Keween­ awan series, rather than above it, the major division between the Cambrian and the pre-Cambrian should be placed at the base of the Keweenawan series. Other geologists believe that at least the upper Keweenawan should be classified as Cam­ brian. 5 The main arguments for the Cambrian age of the upper Keweenawan sediments are: 1. Both are red sandstones of the same lithologic character• 2. No basal conglomerate to the Cambrian against the upper Keweenawan has been discovered; whereas, there is a very thick one at the base of the upper Kewee­ nawan containing a wide variety of pebbles of the intrusives as well as eztrusives of the lower Kewee­ nawan . Some of the arguments against the idea of the Cambrian age of the upper Keweenawan are: 1. The unconformable overlap of the Potsdam sandstone of upper-Cambrian age on the upper Keweenawan. 2. The lack of fossils. 3. The presence of pebbles of Keweenawan in the Cambrian along the Keweenawan fault shore cliff. General Stratigraphy: In the writer*s opinion, Irving’s* division of the Kewee- * Irving, R.D., "The Copper Bearing Rocks of Lake Superior,” United States Geological Survey, Monograph 5 (1883). nawan series into upper and lower is more logical than the divisions suggested by various other geologists, because it is based on the fact that the upper Keweenawan is devoid of any evidences of igneous activity and is composed wholly of clastic sediments. The lower Keweenawan, on the other hand, 6 is composed mostly of a succession of basic lava flows in­ terstratified with sediments* Belov/ is a generalized stratigraphic column of the Ke­ weenawan rocks (after A.C. Lane and A.E. Seaman)*: * Lane, A.C., and Seaman, A .S., ,fNotes on the Geological Section of Michigan? Part I. The Preordovician, Report of the State Board of Geological Survey of Michigan, p. 24 (1908). Name of formation or group_________ Thickness in feet General characteristics ________________________ Upper Keweenawan Freda Sandstone 900-(?) Red sandstone with some felsite and basic igneous debris Nonesuch Shale 350 to 600 Bark fissile shale beds with some sandstone Outer Conglomerate 1,000 to 3,500 Coarse felsite conglomerate, some sandy lenses Lower Keweenawan Lake Shore Traps 400 to 1,800 Basaltic lavas with upper amygdaloidal parts Great Conglomerate 340 to 2,200 Coarse felsite conglomerate Eagle River Group 1,417 to 2,400 Mostly basic lava flows with frequent sedimentary beds Ashbed Group 1,456 to 2,400 Mainly basic lava flows with 50 feet of conglomerate Central Mine Group 3,823 to 25,000 Mainly basic lavas with copper bearing conglomerate zones Bohemian Range Group (?) to 9,500 Mainly basic lava flows with intrusive gabbro; some conglomerate beds 7 Sedimentary Hocks; The sedimentary rocks are subordin­ ate in the lower Keweenawan series; but they constitute the entire thickness of the upper series where they are composed of conglomerate, sandstone, and shale. The sediments are predominantly red in color, feldspathic, and poorly sorted. They exhibit ripple marks, cross­ bedding, and mud cracks; and so far as knoxvn, are devoid of fossils. According to Lane*, their characteristics indicate * Lane, A.G., "The Keweenawan Series of Michigan," Michigan Geological Survey, Publication 6 (Geol. Series 4), 2 vol., 983 pp.' (1911) . . that they were deposited largely under terrestrial conditions. The conglomerates are composed mainly of felsite clasts, and range in thickness from a few inches to 3,500 feet. Some zones have been traced by geologists many miles along the strike. The conglomerates form a very small proportion of the lower Keweenawan and a large proportion of the upper Ke­ weenawan. In general, the felsite conglomerates are of silicious composition, the most abundant rocks in them being felsite and quartz porphyry, although basic pebbles occur in minor quantities. Most of the pebbles are well rounded. The con­ glomerate beds are generally lenticular, thinning or thicken­ ing rather rapidly along the strike. The coarser material, with boulders rarely exceeding a foot in diameter, is usually found in rather thick beds. At the top of the Keweenawan series occur the Nonesuch 8 shale and the Freda sandstone formations. The Nonesuch for­ mation consists of black and red shales interstratified with layers of red sandstone. The Freda sandstone which represents the uppermost member of the Keweenawan series is mainly a red sandstone with some felsite and basic igneous rock debris. Source of the Sediments: The composition of material of the felsite conglomerate and the sandstones is similar to that of several masses of felsite and acidic porphyries that out­ crop in the area. These and other old masses that have been eroded probably acted as a source of the sediments. A.C. Lane* and others have suggested that certain exten- * Lane, A.C., "The Keweenawan Series of Michigan," Michigan G-eoiogieal Survey, Publication 6 (Geol. Series 4), 2 vol., 983 pp. (1911). sive acid flows immediately succumbed to erosion, forming a nearly contemporaneous conglomerate and sandstone. Butler and Burbank* suggested that the conglomerate pebbles were not *Butler, B.S., Burbank, W.S., and Collaborators, "The Copper Deposits of Michigan," United States Geological Survey, Prof. Paper 144 (1929). of immediate local derivations, but came from long-lived up­ lands composed raainly of felsite and quartz porphyry. They infer that the debris from these uplands, together with a small proportion of other material from different sources, was spread on the adjacent plains occupied by the basic lava 9 flows. The Porcupine Mountains area is an example of such an upland. The Igneous Rocks: The igneous rocks are divided pri­ marily into two classes; namely, the basic flows and the acid porphyries. The basic flows make up the greater part of the Kewee­ nawan series. rocks. These are fine grained, basaltic, crystalline They consist of a lower compact portion that grades upwards into vesicular and amygdaloidal parts. The flows are interstratified with layers of unaltered red sandstone and conglomerate. The basic flows are true eruptives and constitute successive flows from fissures. This suggestion was introduced by Irving* and later accepted by various * Irving, R.D., "The Copper Bearing Rocks of Lake Superior,tf United States Geological Survey, Monograph 5 , p. 139 (1883). other geologists. The acid rocks like the basic, are true eruptives, main­ ly porphyritic, and occur between layers of basic rocks. Structure: The Keweenawan series in Michigan occur on the southern rim of the Lake Superior syncline or basin. But­ ler and Burbank* suggest that this basin was probably formed * Butler, B.S., Burbank, W.S., and Collaborators, "The Copper Deposits of Michigan,” United States Geological Survey, Prof. Paper 144 (1929). 10 during Keweenawan time. The lower Keweenawan rooks dip steeply, and the upper ones dip progressively less steeply northwestwardly towards the center of the Lake Superior ba­ sin. The Keweenawan rooks are faulted. The greatest fault in the region is the Keweenaw fault which bounds the Kewee­ nawan series on the south from Keweenaw Point to Lake Goge­ bic. It is a thrust fault with a northwesterly dip, along which the basaltic series have been shoved over the Lake Superior sandstone of upper Cambrian age. There is very little discordance between the dip of the fault and the dip of the beds of the flows. Many branch faults and fissures are associated with the Keweenaw fault. Butler and Burbank* * Butler, B.S., Burbank, W.S., and Collaborators, "The Copper Deposits of Michigan," United States Geological Survey, Prof. Paper 144 (1929). suggested that the movement along the Keweenaw fault probably did not begin until late Keweenawan time, much of it occur­ ring after the Lake Superior sandstone was deposited. Ore Deposits in the Keweenawan Rocks: In Michigan, the area of exposed Keweenawan rocks was one of the greatest cop­ per districts of the world and outstanding in the deposits of native copper. This area forms a belt in the Keweenaw Penin­ sula two to four miles wide and 100 miles long, 26 miles of which has been highly productive. This district is now almost exhausted. The copper lodes are of three types: (1) amygdaloidal, 11 which occur in the upper permeable parts of flows. copper occupies the vesicles. Native The lodes average 13 feet in thickness and contain from 0.6 to 1.5 per cent copper, (2) the conglomeratic lodes, in which native copper fills the interstices, (3) fissure veins, in which the native copper occurs in fissures and joints. Butler, Burbank and other geologists consider that the copper deposits were formed by hydrothermal solutions given off from underlying basic intrusives. They believe that the structure is pre-ore in origin, and that the relations of copper beneath impervious cappings indicate rising rather than descending solutions. The solutions rich in copper, sulphur, and arsenic were guided upward by the permeabil­ ity of the conglomerates and amygdaloidal tops. The hema­ tite of the lava tops yielded oxygen which combined with the sulphur and arsenic, causing reduction of copper to native metal. General Structure of the Porcupine Mountains: In the Porcupine Mountains the succession of rocks and their struc­ ture do not conform exactly with the structure of the Kewee­ nawan rocks to the northeast and the southwest. In their geologic map of the Porcupine Mountains and vicinity, F.E. Wright and A.C. Lane* indicated the existence of a large * Wright, F.E., and Lane, A.C., Preliminary G-eological Map of the Porcupine Mountains and Vicinity, Michigan Geological Survey Rept. for 1908, pi. 1 (1909). 12 fold with a general northeasterly trend. The general struc­ ture is, moreover, complicated by the existence of numerous transverse and cross faults. The most prominent fault is the Main Porcupine Fault that borders the southern edge of the main felsite (Red Rock) area which forms the central portion of the Porcupine Mountains. Here the Red Rock is in direct contact with the Nonesuch shale. The Main Porcupine Fault is a transverse fault with a general northeasterly trend. According to Wright and Lane*, it extends from sec. 1, * Wright, F.K., and Lane, A.C., Preliminary Geological Map of the Porcupine Mountains and Vicinity, Michigan Geological Survey Rept. for 1908, pi. 1 (1909). T. 50 N . , R. 42 W . , westwards to sec. 7, T. 50 N., R. 42 W . , and thence southwestwards to sec. 18, T. 49 N., R. 43 17. Any relation between this fault and the Keweenaw Fault has yet to be established. The detailed geology of the Porcupine Mountains is still in the most part unknown. More extensive field work is needed to throw more light on the problem. Moreover, attempts at the correlation of the numerous core drilling data which exist will lead to a much clearer picture of the Porcupine Mountains problem. 13 Stratigraphy of the Porcupine Mountains; Following is a generalized stratigraphic column of the Porcupine Moun­ tains area. The information given here was taken mostly from Irving*, with some modifications by the writer. * Irving, B.D., "The Copper Bearing Rocks of Lake Superior," United States Geological Survey, Monograph 5 (1883). Name of formation Description of formation Thickness in feet Upper Keweenawan Nonesuch Shale Gray shale and dark sandstone 600 Porcupine Moun­ tains Sandstone Sandstone with thin conglomerate zones 1,500 to (?) Lowe 2? Keweenawan Lake Shore Traps Basaltic flows, amygdaloidal at top 300 to 500 (?) Sandstone and conglomerate 1,900 (?) Diabase, melaphyre, amygdaloids, diabase porphyry, one bed of porphyry-conglomerate 400 Red Rock(?) Felsites and quartziferous porphyries, banded rhyolite (?) All the above formations, with the exception of the Red Rock, show a general northeasterly trend and northwesterly dip, except in an area along the Iron River about one mile south of the Lake Superior shore. Here the outcropping 14 Nonesuch shale exhibits marked anomalies in strike and dip indicating the probability of the existence of the "nose" of the main fold in that area. On the other hand, these anom­ alies in strike and dip might be as a result of the faulting. The Red Rock, according to Irving*, shows no apparent * Irving, R.D., "The Copper Bearing Rocks of Lake Superior," United States Geological Survey, Monograph 5 (1883). trends; but Thaden*, who spent the summer season of 1949 * Thaden, R.R., Personal communication studying the Red Rock in the field, disagrees with Irving’s conclusions. inite trends. Thaden indicated that the Red Rock exhibits def' He also observed that the exposed contacts of the Red Rock with the basaltic lava flows are faulted. The reader, however, has to be content with this statement un­ supplemented by evidence until the full text of Thaden* s paper on the Red Rock is completed. 4. Purpose of Study The purpose of this paper is to report the structure and petrology of exposed sandstones and conglomerates in the northern part of the Porcupine Mountains along assigned tra­ verses, and to investigate the possibilities of correlations of these rocks between the traverses. The traverses along which the writer studied and sam­ pled these rocks were confined to that sedimentary formation 15 stratigraphically above the Lake Shore Traps formation (Map 2). On Plate 14 accompanying the United States Geo­ logical Survey Professional Paper 144, the name assigned to the formation is the Outer conglomerate. This name was first given to the formation by Irving*. He suggested that * Irving, R.D*, "The Copper Bearing Rocks of Lake Superior," United States Geological Survey, Monograph 5 (1883). since it lies directly above the Lake Shore Traps, it was cor related with the Outer Copper Harbor conglomerate that out­ crops in the Keweenaw Peninsula, and which also lies directly above the Lake Shore Traps. The Outer conglomerate in the Keweenaw Peninsula is composed essentially of coarse conglom­ erate with thin lenses of sandstone, and the name seems des­ criptively appropriate. Gordon* described the Outer conglom- * Gordon, W.C., and Lane, A.C., "A Geological Section Prom Bessemer Down Black River," Michigan Geological Survey Rept. for 1906, pp. 597-507, map (1907). erate along the Black River section southwest of the Porcupine Mountains. Here the lower two-thirds of the formation is coarse conglomerate, and the upper one-third is sandstone. In the northern part of the Porcupine Mountains, the writer found the majority of the outcrops to be sandstones with thin zones of conglomerate. It may be argued that the exposed rocks along the traverses comprise only a small percentage as compared to the unexposed rocks; thus, the unexposed rocks 16 might be conglomerates rather than sandstones. From his observations in the field, the writer noted that the con­ glomerate zones are more resistant to weathering than are the sandstone zones, and they occur in the form of knobs and prominent ridges (Figure 1) as contrasted with the sand­ stone outcrops that lie adjacent to the surface of the ground (Figure 2). Thus, if the rocks in the area were mostly con­ glomerate, more knobs and ridges would have observed. It is, therefore, inferred by the writer that along the traverses the rock is mostly sandstone with subordinate zones of con­ glomerate . Dr. W.A* Kelly* of the Department of Geology, Michigan * Kelly, W.A., Personal communication State College, pointed out that since the writer found more sandstone than conglomerate, the name Outer conglomerate seems very inappropriate and is misleading to the reader. Moreover, even though the formation lies directly above the Lake Shore Traps, it might not be the same formation as the Outer Copper Harbor conglomerate. Also, the name Outer conglomerate is inappropriate since it signifies no geographical locality. Dr. Kelly suggested the name Porcupine Mountains Sandstone for that sandstone formation in the Porcupine Mountains that lies stratigraphically above and in contact with the Lake Shore Traps. Thus the name: is introduced in this paper* Porcupine Mountains Sandstone Figure 1* A typical conglomerate knob. Note the sandstone lens contained. Figure ^ * A typical bedded sandstone outcrop adjacent to the ground level. 17 18 PROCEDURE 1. Field Procedure The field work of this study was completed in the sum­ mer of 1949. Six traverse lines or sections, perpendicular to the general strike of the Porcupine Mountains Sandstone, were assigned and traversed (Map 2). mainly by pace and compass. Traversing was done Along Section I where the brush was scanty, distances were measured with a steel tape. In other locations where the brush was very thick and accurate pacing or taping was impossible, the position of the outcrops was located by the use of aerial photographs. Samples were collected from outcrops along the traverses. Where exposed rocks were continuous, samples were collected from the different lithologic zones. Strike and dip of bed­ ding as well as prominent joints and other primary structures were observed, measured, and recorded. 2. Laboratory Procedure In the laboratory, the samples were examined with the aid of a binocular microscope. Their descriptions are tab­ ulated in the appendix accompanying this paper. Pebbles collected from the different conglomerate zones were classi­ fied and tabulated. Exact mineral and petrographic determinations of the sandstones were made by examining selected thin sections. Also thin sections of type samples of the pebbles were exam­ ined and classified. 19 Sandstone grain size classifications in this paper follow the standards of the United States Bureau of Soils: -- .05-.10 mm -- .10-.25 mm -- .25-.50 mm .50- 1.0 mm -1.0 mm and - 1. Very fine grained 2. Fine grained 3. Medium grained 4. Coarse grained 5. Gravel up Sphericity and roundness measurements were made on the pebbles and sand grains by the visual quantitative methods described by G. Rittenhouse* and W.C. Krumbein**. * Rittenhouse, G . , ”A Visual Method of Estimating Two-dimen­ sional Sphericity,” Journal of Sedimentary Petrology, Vol. 1 3 , pp. 79-81, abstract (1943). **Krumbein, W.C., "Measurement and Geological Significance of Shape and Roundness of Sedimentary Particles,” Journal of Sedimentary Petrology, Vol. 1 1 , pp. 68-69, plate 1, ab­ stract (1941). To determine the sphericity and roundness of the sand grains, a portion of each sandstone sample was crushed, and the loose grains examined under a binocular microscope. Ten grains were picked at random, and their sphericity and round ness were determined by comparing their two-dimensional images seen under the microscope with the images of standard grains and pebbles reproduced in the two charts of Ritten­ house and Krumbein. The calculated average sphericity and roundness of the ten grains for each sample, together with the sphericity and roundness of the pebbles, are tabulated in the appendix* £0 An attempt was made to correlate the exposed rocks along the traverses by means of: 1. The distinct lithologic characteristics of the outcrops. £. The sphericity and roundness of the sand grains. 21 © © d d O O © d o rd © © d p o (M in © O d 0 rH 1 o •H +3 O 0 o •rH P d o o H? o p CO ■d to d d £ CO d o f—t •H Eh o Eh d d d EH Pa I—I d p d O d o d W 01 •H o •H O d o •H P d o o rH d o •rH P o © CO © d Eh •H P O 0 CO d P d d p © o •H w d £ tiD d d o •rH d d o O d c(h M © Oh Eh • d O •rH d © Oh © d o d co d © C a O o d d d id {>> d o © d d EjD o d d d o o © w d o o © d p tiD d £ o rH i—1 o 3-H i— 1 Oh d d Eh d O d co 0 M d d © d d d £ © d O d co © M d id i-l h4 Ul w d t> d i— 1 d i> d (— l d w > d d i— 1 d rH i— I d — d rH •rH i— 1 O i— 10 d rH d Oh C iD 0 >5 d rH d d •H O rH d d E*0 rH d d •H O i— 1 d d tdj i— 1 d d C Q •H i— { O i— 1© d rH d Oh «jo £ >5 d S CO © ,— » m Oh d d Eh P3 b a <*5 b s w i> ^ CO & < 0 © © d O © t> d d P © d d © d © d P o p d © d •ri P d o o 0 d 0 £ © Oh O d o p d o J3 © p p d w © p d © O •rH < p o © d d p d > d © w *"' d d d d H d £ 0 © © Oh o g o p d O W * d © d O d C O © W d H d O *rl d d u O P d o 0 d Oh d CO i —I i—I o 10 § o p d © d +3 § d —» interval O -• © Oh d d EH Concealed <5h — -— » © Oh d d EH d &H *H o d O o 0 d 0 Oh O i—I co i O rH O o I—t • F3 ld d © P d rH d d d P E aD d * Cl 0 P d •rH d 0 rH d 0 O g t g o dt) i —1 o 0< — *H M fciOd g cd d d dd o o O 0 CO o OOpq i 1H CM • • CM O o o o in rH d • d CQ cd 0 M O O - H H* * H Ph P p •— * Cd W S CD P-t H 0 •• g 00 0 d rH i 1 *H CM in • I— I 0 g 0 co — l> PH 0 P d fh *H d 0 H 0 0 o d o o in > PH 0 0 ^40 *h in p w 0 d *• 00 O P 0 H d d d dd *— ^ cH 0 rH CM P d *H d 0 H 0 0 d d 0 Bearing Distance in feet Position • 0 > PH © P CQ O *H P d 0 00 Ph H 0 g 0 O H h cm O o o ttOg d 0 O CO O o• o IQ IQ in • CM 0 0 CO fQ I— 1 g 0 CO O in Ph O o o • ig: CM LQ r— 1 • # • in 1 "vH 00 00 d 0 i—1 0 0 O d o o o CM 0 05 H O p 0 0 1— 1 Cm d CQ H CD 1 o co in 1 cD i o d © H 0 0 O d g d d 0 0 00 o o CO * —' IQ • iH o IQ * o tQ H • to o 1— 1 d ■rH £3 G> CM 0 > Ph 0 P •H £3 o o H P d •rH 0 • • CM CQ H d o o o H 0 * o p CQ * i— i 0 O — 00d d d o 0 o fQ d o o in CO cD CO • o 0 n 0 0 0 do 0 CQ O •H P 03 SH 0 0 in 00 p CQ • m CQ to 05 1 00 in S3 © d O P 0 d « C O CQ • * is i— s cO > 0 p '— cd o P hC V 2 0 i— | Qh <30 £ d C O O 03 O ■ to Position Distance in feet Bearing Slope Remarks © Thickness in feet a O rH • CO 11 — Fh 0 -P d •H d 0 rH cO 0 o d o o o oa o 0 o to a i> O CO • p 13 • 0 d *3 ~ a O 0 0 tO (0 ^4 W •H o Fh Oh •H P *H P Wd rH 0 Oi Fh « « 0 0 S ttD i— 1 o d 1 — I •H 2* tiDd 0 d d O 0 C /D PQ & o LO ♦ CO to rH o o i—! « pej • o O o C V J • o CO « S3 i— i £ t> Fh 0 P d •H d 0 i— 1 0 0 O d o o o o 0 0 o• to 1 • *2: o o « S3 d < m o P •H — i 1 o rH 1 05 cs O- rH rH 1 o 1—1 o o ^ to C O • '3 « S3 ** O r-H 0 ^ 0 J^i 03 rH d Fh Fh Oh O d O) ® P -H -P +3 0 d 0 0 0 rH 0 A4 Fh «• 0 d O o 0 g ttf) 0 F h O d rH p 0 o rH -H O, d trfjd g d d d d 0 C O 0 d O 0 O pq — CO rH H • O •H P 0 Fh 0 6 o rH W )P d d o 0 o 0 0 O O pH 0 Fh -P El o •H P 0 O o pi 0 0 0 CM a o o d o Fh Cm *0 0 0 m rd El 0 +3 0 03 Oh 0i Ej O d £ o ,0 0 0 0 M 1 —I El O *H P O 0 CO 0 O j•> O 0 CO «• H M 0 O *H P O 0 to 0 O 0 EM HD 0 O i —1 0 <1 0 0 Fh 0 > 0 Fh P • Fh O «H Et 0 EM 0 CO 0 0 P 0 0 0 a 0 Fh O fEj 0 0 0 -P 0 O El O •H P 0 O o 1 —1 0 o •rH -P 0 o o PI 0 0 Eh o -p EN o rH 1 fcr^t fiizi 0 M Fh 0 3 0 C0 0 0 0 P 0 © 0 0 O

H (H • 0 O pc)0 O *H 0 IQ *H p P O rH p Fh •H LQ Fh 0 O D- ♦ 0 > 0 • " O g • « • o •^ >5 0 E>- ^ q 0 03 o J *H O LQ P 0 EM CO ^ 0 P *H O 0 0 • • cO -— 0 rH 0 ** O HD *• 0 P 0 0 rH 0 *H p CL, 0 0 0 0 0 0 *H 0 0 0 O CO O pq 1-3 i —1 0 > 0 0 p 0 •H o o • cr> •i —1 i —i do © • o o o pqo -H GO -H ---P 0 O i — 1 Fh CM Fh 0 CO 0 *H 0 O O- • E> 0 > P 13 0 • « ~ « 0 « • • • 0 o & pPj E2 0 0 tO 0 0 030 O O •H O O O o fh em lo ca co •H p «iH p 0] 0 ♦ • • 0 S CO C0-— * 0 03 0 •• £ HD *• 0 O 0 0 rH rH *H p EM HD0 0 g 0 0 *H 0 O 0 O CO O pq K> 0 0 •H © > > 0 © i —I 0 0 O 0 O o to LQ • 03 i —1 0 !> 0 0 -P 0 •H P 0 i —1 0 0 O 0 O O 0 P •rH O i —1 0 O 1>3 0 P 0 O * 0 CO 0 O 0 P rH 0 CM ■0 & 0 0 0 CO co'— o o • to o 0 0 Fh O o 0 Fh m 0 £ • 0 O •i—1 P o 0 0 0 •H r0 P HD 0 o 1 —1 0 0 0 -jO o 0 ■0 0 o o 0 0 P 0 0 0 0 0 P cm I o 1 —1 CO O O i —1 o o • HD 0 •H U 0 0 PQ o o l • o o • • S3 LQ #s 03 o CD rH 03 1 r —1 CO 1 03 0 0 •H HD 0 •rH o 1 —I i —! O Pm 0 O 0 0 P 0 •H 0 O •rH P ♦H 0 o PH P 0 0 fh 0 -P d •H Remarks o in Slope o d o o Thickness in feet d 0 rH cd 0 • 0 0 d o •* 0 P 0 i— I 0 +3 On d d S d -h 0 0 o CO CO t~3 LO • CO Bearing Distance in feet d l> Ph 0 -P d •rH 0 0 *0 0 rH 0 0 O d o o o to •d d rH •» o CQ CO > Fh 0 P d •rH o O •H 0 -P p 0 0 Fh Fh 0 0 0 d o S o o P 1 —1rH 0 CiD tiDd d d d 0 • co o- 0 d O O C Q b 0 0 0 O d o o tO O to ♦ • • to i —1o o LO & o o 0 0 ** 0 W rH P 04 d a *h 0 o co rH t> «. A • • 0 Fh s •• 0 P d *h o tr—^ co o rH 0 rH CH 6 0 CO 0 P d •rH d 0 rH 0 0 O d o CO r-D "•—* o o* to Fh 0 O to I> rH 0 d O P 0 d d 0 > > o o • 1— 1 0 i— i o v- i—1 0 rH d o © P rH 0 CM d £ d 0 0 co CO— LO • CQ o LO o o )—1 • ♦ o o • !3 « F2* o o • !s o o • o o • 13 co CO < —1 o GO sh 1 to LO 1 1 'nH o LO P d •rH d 0 i—1 0 © O d o o o 03 o Id o o • Position 0 0 > 03 p i— i 0 0 > -— rH 03 to 269 0 > •H »H P P Fh Fh t■ o in t1 > to 7-8 1 —1 0 d o '— *• to Ph od ^ *— 1 * d d tjD 0 0 O Fh O Fh tO in •rH P Fh 0 3.5 d. o 1— 11 —1 0 0 o o 5° 1 —1 0 o N. 0° W. W) d rH •H cd Conglomeratic sandstone Bedding: strike N. 71° E. dip 27°, N. 19° W (Sample 12) 25 26 W d *rH © t> © P d d •rH O © © •rH ■id M © 0 * 0 © ft| 0 H Ph OP O O 02 Fh O © rH © • © o •H -P Ph © • M O o ©O CQ do ocs 1— 1 © > JH © P Slope Thickness in feet Remarks d »i*4 d © rH © © O © d o • -p ^ © • d ;z; ~ d o © © © CO tfl,y w •H O Ph 04 •rH p * rH +3 © d - — © PH © •• £ tt) o d i— 1 «H tiDd d o o dd o © o PQ LQ rH LO • CQ O LQ i— 1 CQ r—I © H 04 £ © CO — J> Fh © -P d ♦H d © i— 1 © © o d o o LO rH -p © d d © © * I— 1 © > u © -p d M o LO CQ o •H -P ' ^ •rH -P Ph rH © £ © O rH d © rH © Ph rH © £3 ** © O © rH rH H ft dD d S d *h © ©^ (— 1 «) s d © o co O — o• IQ © © CO LO © O d o o o O CO o v-3 *■— ' LO o• to CQ O o LO Bearing o • 13 o o • 13 P d > o rH • • O O K*i d 1— t O o • d d g o Distance in feet Position 05 1 co O rH -P d © -P d © rH © © O d o o Ph CO rH © • ®1 —1 d t> © © © CO © d g •• d ttO •« © © o © i—1 O © rH p © -p i —I © p © d © rH -H p CH*H d ra o, © d g d ftd d a © d o d ftd -h © rH © d © d O CQ © Ph © CO o © -H © o co ph pq Hd — O P CQ— © •H LO rH •rH o• fO © > Ph d •rH ,d © P -H © © d o o LO • 1—I CQ ©> o LO 1 —1 o o • *-a ’ 31 p .* o o • • p=o o • 13 1 05 to i— 1 o i— 1 i— 1 CQ rH 1 o rH - © "P h rd F o © d > © © © e © l> Ph P 05 ^ © O • *rl «N tj£) 13O ~HtO d © LO CQ M • •H CQ O •H 63 S -H o O © O Ph OhlO p O o rH LO • © rH d ^ o * !> nd rH p © > rH •H 02 O M o •rl 05 1 1 1-1 1-1 © O o to rH 1 1 CQ rH d o • O- -H rH 0 Fh o dw 0 rd a o co d o 0 © © Fh © > 0 Fh -P cd o o id o -p p 0 rH 1 0 p © H H H CJ o •rH P o 0 CO M M M d O *rH P O © CQ ■— 1 0 i> Fh © w Oh P © © 0 dr a o O i= ^i r“i 0 £ d EiD •H w d o m d o •rH -P 0 o o d a o Fh V CQ d d d rH • O P P w • d s O —* • d 0 © ■vfC Fh © P d •H d © © rH rH 0 Oh © C 3 0 d CQ o *—' o o I —1 d d d d 0 © 0 © M CM •• •H O Fh O n d © •rH P •rH -P P © d CO 0 0 © Fh Fh © • • w d © o a a taD © rH p o o d O tO CQHrHP d EiD CiDd d d dd 0 o o © cq o o pq IQ003 • O * • rH O Eh -H © Oh O i —I CQ O o o O rH Fh d © P 0 i —I d d 0 P 0 w •H E a O d •H £ O i— 1 i —1 o P«4 o o C\3 d •H Fh 0 © © O P d © 0 © P Vh ra •H d Q d d to o dd o *H p •rH P O O *-1 hH 1 — 1 C M 1 rH 0 o o o 0 o LO d d o •H p •rH w o Ph CQ 1 (M Oh a 0 3 Concealed H H H d o •H P O 0 CQ EiD d o interval 27 LO 28 MO C O 0)0 i— t cl 02 O O • +? a C Q • Cl O © P h © P C| •H d © i— I — od Qt © o a cd d CQ o o ■ — o 1— 1 rH O d > Bearing Distance in feet Position • cd .—» a © © P d ■ —» •H © t> d o © P <-4 C Q d S d © rH Oh d cd cd CQ CQ od © o d o o • 02 O O i —1 • o o ♦ d o d © © P p © © C O P h F h © © © a a © O O rH i 11 1 i— I © > F h © P d •H d © i— l © — — CM © o tdDtiD3 d d d © o O CQ o o o *■— o LO LO D- • O O © d o 4-3 © d d O rH • • O rH O o 1— I LO rH © O 02 d 04 o tQ • p is © • d a * o d © © w •H o P h O •r~\ p *H ^ w d -— •P o © rH P h © « © 3 tiD rH O Oh 3 02 M 02 • d i —1 wd dd o © O pq o• o o rH rH © > F h © P o d •H d © rH Oh O F h O P © © O d o o S3 o 1 d O O P -—« . © a\ i— 1 cd !> Fh 0 P d •H d © 0 rH C M E] 0 co 0 i— 1 cd © o d o o IP )— 1 d d © 0 -p < — i © Fh © © d © a O P rH 11 Etfd e d d © CO O CQ^ o 0 — © CM © o o o I— 1 « o 1 1 • • tp • 02 Position Distance in feet Bearing fd o o o • o IP 00 « rH © > F h 0 P d •H d © i ) © — © o d o o 1 • id rH © O O IP 0 © P © ^ Fh > Fh ' 'o i— I 0 E| •* 0 O M rl rH P C M i d d -h © O OC O O Ha " ■ —" ED 00 • o o o « Id o o * 0 0 0 £ P d *H d 0 < — 1 © © o d o o o rH d O P « © --— d 00 d rH © md d o © •H p 4^ £>• © © rH Fh Fh 0 0 m 0 fr = J — 1£ 0 o O i—1 rH rH Cm UO W) e d d © o o co o o 00 IP • • LP o o i— 1 © t> Fh 0 P d •rl d 0 © 0 O d o p C Q d d © CQ o •H P —* © C J> Fh rH 0 ■ — 1 a © O rH rH C M d O o d © 1 tioa o co o LP • 02 IP O O • id ♦ o o • o o c• 13 13 d o o p © o o •rH rH to Cft <£> O o> to f— 1 C O rH 1 1 — 1 1 rH 1 — 1 id rH O rH | C T > i— 1 1 O rH 02 1 — 1 1 rH i— 1 02 co interval 0 P cd Fh 0 d ** a O £jD OP d CQH &I)d d d d d cd 0 1 — 1 © o •iH P F h Concealed • • idO 00 O rH 02 O * Id ♦ .*— ■ * ja «to O rH 0 02 •d 02 d •h d Fh cm cd -p *H Xfl d 02 rH 30 C Q M F h i N 0 d fciD o cl p F h l—I 0 CQ 01 tO • 13 53 o 0 rH * r^i 0O ■p C QP d lo I —I P d i—i I —I O' i—1 0 0 > F h i> >1 • F h P p 13 F h u 0 © 0 O P p * P P d d d •iH m d • *H •H o — •H P d -^ tO 0 H LO Q nd d LO © tO d rH LO i — 1 i —I 0 O P d © 0 0 P 0 •h o o P -H o LO rH o 05 o 00 to d o •rH -P •H 0 o Ph 1 i —1 CO CO I LO rH (— I I tO rH I £> 05 I —I I CO o OQ 31 i —1 od o © d •H © t> •rH P Fh £ ISI P d Fh 0 cd M co O o tH Ph d O' J3 M Fh 0 p d •H d 0 rH cd 0 O d 0 Fh Fh •H f>> Q P d o — *>o 0 d O P 0 d d CO 0 rH Oh g rH 0 t> Fh 0 P d *H d 0 rH cd 0 o cd cd CQ CQ '— ' o o o in co LQ o d LQ rH S3 rH g tjD 0 d rH *H tjDd d d 0 0 0 pq tH 0 1—1 S 0 CQ — ' O 0 CM O 0 • 1 —1 0 S3 Fh 0 P d •H d 0 H 0 0 O d 0 0 ~ O 0 LO JA CM •H Fh Pr p H W 0 d --CM }> 0 d •• 0 £iO p CO•drH d d d d 0 0 CQ PQ IQ « C M 0 LQ d iO © d • rH 0 t> Fh 0 P d •rH © 0 0 O d 0 d d d 0 0 0 0 CQ O 0 rH Or 1— 1 a 0 O •H p 0 Fh 0 S OO 0 rH H H 0 0 0 p 0 Fh 0 0 0 0 t O o o o o o C M OS O to cI —i C M CM CO C M C M C M C M C M C M CM S3 CM I i —I I * • W H W O O i —I C M I O 0 0 1—1 Or 1— 1 0 > Fh 0 P d •H d 0 1 —1 0 0 O d 0 0 LQ LQ O CO O o C M CO CO tiD euD flQ s O O C M co •H p 0 Fh 0 d CQ 0 P d 0 d d 0 d 0 0 p 0 d d 0 0 O O CM rH Os © *• O O O CM LQ o CM I 0 O CM d o o t> • P fen 0 * d ^ * d o 0 0 CM 0 ,M CM •rl O Fh 04 •H P *rH —^ +5 0 d H 0 Fh IO LQ IQ O Position • d p S3 0 o od © p •h rarH 0 od Bearing Thickness in feet (S o 3> 0 © I^o £30 I co tQ 32 d d © d © ai O P o CQ X P g s © p=; © d o -p ra d cl © w o •H +3 — © cd Fh tO © a © O rH i —I Oh W) S cl © O CO O E^O 02 o OJ CO cD • la 1 —1 8? I> Fh © 02 o- -©p Cl •iH -©px-. © CO Fh cq © d © O f—1 i —1 Oh ( —1 © t> P © -p cl rH © > Fh © -P d la o ©^ M 02 •H Fh O h +3 *H ©d O © •• © o CjD © -p •rH d i—1 Oh © fi d d d d © © © CO co pq ^ o •rl © CQ d © d o © 1—1 ■p i—I © W Oh © d B o d d © © co o CO " o 02 • tO O 02 rH C\2 O O 02 02 o o 02 O O 02 O o 02 o o O O O O la la la o 05 lO o 02 05 Di CD 02 co 05 02 I CO d © rH © © O d © d O •• CQ o tiD © i—1 -p d © d © •rH d d o o d 'c* © © CQ pq cO * la p Fh O h d co O rH 1 —1 © o t© M 02 •H © •H pao d © rH © © 2 ? O m © d CO o o W 0 d © •rH d © © © rH O d o co o **—- o 05 i—1 © > Fh © d •H d © i—1 © © o d o o Outcrops of conglomeratic 25 feet off shore sandstone d (D © © Oh O rH CO o • C a O d •H P © © pq O o • 13 o CD CQ • o o ♦ © O +3 d © © © w -p (p •h d pq *h CQ 02 — i1 cD cD o CO 0° © 02 N. 0° W* d © Eh *P o* Location 8 d © M © O a cd M 0 d O © Fh o d 0 0 d w 0 t o o Fh 0 P d •H o © d Fh © P d •rH d 0 rH 0 0 O d o o . —0 t>d O 0 P rH 0 o, d fi d 0 0 CO CQ^- ^ LO • CO N 0 • rH * 0O O LO • •H C" txlO P Fh CmO d to • Oh •H Fh N -P o o © i —i o d o pq Fh I t M> o 0 d © i —1 0 0 O d o o © d o p 0 d d 0 CO O LO CM o- CM •• tiD d •H d d 0 PQ to 0 i —1 O E! 0 CO *"— o < } h •H d d o o o • • * CO rH rH * Cft 0 0 o •rH P 0 O d o d Fh O o d a o •rH P O 0 Fh •H d Fh O LO CM 0 CO > 0 H d o o pq 0 d d 0 P X M d • •rH P o 0 CO • d •H 0 O d © d p -p o 0 CO d d 0 o © Fh d 0 p 0 — iI d d 0 p 0 0 •rH tiD d •H £ O i —1 i —1 o £h d 0 I —1 0 0 o d o o 0 0 0P d 0 d 0 Eh *H d o i-4 0 > Fh 0 P d •H 0 CM O rH I o o I CM CO • tiD d •rH Fh 0 0 1 PQ 0 O d © 0 0 P d 0 -p d »H d 0 rH 0 0 0 d 0 0 0 d 0 -p 0 d d 0 0 0 •H -P 0 d OI 0 a 0 O rH rH O h w s d 0 0 co O'— 1 —1 0 > d 0 -P d •H d 0 rH 0 0 O d 0 0 LQ 00 • I-1 O LO rH 0 02 rH 0 O •H -P 0 d d 0 0 > -p 0 « d * d^ 0 00 LQ O tO P 0 13 O d rH 0 •• 0 O 03H rl -P O h tdDd & d *h 0 0 O CO Ob'-' O CQ O LQ rH • • • • i^• • Bearing Distance in feet Position m 0 in 1 —1 0 I> d 0 -P d •r-f d 0 1 —1 0 0 O d 0 0 LQ CQ CQ • d ~ d 0 0 0 CQ 0 ^ 02 •H O d Oh *H p *H p 0 d-—' 0 rH d H © •• S W 0 d 1 — 1*H CiDd d d 00 0 pq 0 • 02 0 1 —1 Qh g 0 co — n 0 d 0 p 0 rH 0 > d 0 P d •H d d 0 0 0 P 0 0 0 02 d rH 0 £ 0 O rH 1 — I O4 d d 0 0 0 d 0 1 —I 0 0 0 CQ a 0 co • 1 —1 0 0 LQ 1 —I LQ rH • • P4 0 in 02 0 LQ 02 # CO 02 02 • CO • CO • CO to CO LQ 1 —1 rH 1—1 02 1 L|Q 1 O■ LQ £>11 tO CO O d 0 F40 LQ 0 O 02 d LQ O to • -p 3 P4 0 rH CO 1 t> 1—1 0 t> d 0 P d *rH d 0 1 —1 0 0 O d 0 0 0 0 r—i 35 t^O to (DO W O 'O • is do ■p CO • © d o ■p © rH d rH cd W M CQ •rH u d © p •d is d o ~ Slope Thickness in feet Remarks O FH CH •H -P *H -p CO d cd to -P d d H d o d © — ii iH d o CO (D ** S tiD < — 1*rH tiDd d © o pq B © © cd © o d o o rH • O o rH O •H -P ■ — cd ^ d rH © B ttf a d cd o co O'— LO CO • C\3 LO LO 'sM 1 CO t> > -— CQ tt) d O rH © Superior © 03 Fh © > © Fh P of Lake 03 © © O h 6 O O shore d d cd 11 on the © o cd CLi © P P o d Fh O O © Fh Location O TO ^ Fh © H © Pi © d d © Od P d #%*»•« w © ♦ • • d d p d i ^ ^ d © 03 © 03 03 o o o O o o o in h cd o O Fh •H O © p P LO Fh © Fh m © d © B O g ** rH OP O W iH 03 rH P tiDd tiD d B d d d *h o © o — o c a o b rH © O •H **rH o © LO O C s -~*rH P © Oh Fh a *H © O d J> P C Q d • • d |=q ^ © ©o o O LO O W tjL ■iH wo • • • 0\ ■p * • © •*© s S3 CQ © £5 S3-—» Fh © © 0 • • © o © CQ O 03 rH P tiD d d *H o o O d eg P © F h d © O }> p C Q «. d ^• d © rH Oh © CQ *—' to LO d O H* d •H © P • © s; eg © Fh 03 d o s •• © p O 03 rH © © H P d tiD a £ d d *H © © O O C Q O b *"— CQ do eg d co © tO • . S3 i— 1 • © S •* rH O H © eg © M eg Fh -H © Fh Oh 04 P *H w d © d •• O tiD p d W *H d d d d © © CQ pq W CQ ©P d © ^4 © oP •H p d Eh -H to ©a * 4 lo * i— I i— Io I —I to LO CD O • • eg H LO * © Oh O CQ d 0 p cd from V extends Section P tiD d •H d d © P I w 03 • O ^ Fh • O i—i d P cd p ♦ eg 04 © S3 d o d £ o p w 03 © cd W •H tD d •H £ O i — I i — 1 o Ph w •H Fh © © PQ © OP d © © © P 03 •rH d PQ »H p o to LO tO O LO to CQ CQ CQ o o o o eg I CQ LO d d rH rH O P © o o •rH rH LO LO id d o •H P *H 03 O Ph rH rH I eg I CQ rH © i—I & B © CQ 37 * 1 —11 —11 —I 0 0 0 o o o •H «H *H -P -P -P Fh F h F h 0 0 0 t> 1> t> to rH «s • • ^ (x! ^ -—. 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A •V ** • • 02 O S 02 © ^ 0 © M 020 ( •H O O © © Pu<£> 02 © O p *H •H Q rH P P C o o © © 0 © *• tj£) 3 © rH 1 — 1•H e*o fciDf© © © © © O O LO 02 O » r 102 • O JS 02 rH © O O TO o o © LO CO © © © P > > © * *05 © CO rH © P •H © © S •• © rH P w © © *H © © rH © © O © o O © o o O LO LO # H o o O o 02 co © 1 — 1 3 © 3 © © o p 03 © © © © interval & > H © > F h © P © © Bearing Distance in feet Position • o LO 02 El o o o O • — o 02 02 • • CO CO 05 «£> o o LO 02 • C O 05 O •H 1 05 rH i— 1 1 o rH o LO 02 • co 05 C O CO 02 i— 1 1 rH rH * !3 © © © m o LO 02 • rH rH ,'S © © • O o &3Q •© •H IO P P iO 02 © © to © © tO * t> t> Concealed rH rH © o •H P © © > > — © © o +3 03 r© © © 03 • F30 i 1 ©O 02 © 05 o © * -p S3 co • © & « © © © C J O C Q^ 02 •H © F h •H -P *H p C Q - rH © O •H -P C O 1I — 1 02 rH pq © • • S2© ** c q p © *H O ha 03 © rH Oh 3 © CO 39 CQ to • N • PQO LO O c\2 LO !£> • 1 — 1 d d © C C S Slope Thickness in feet Remarks P to cd c\2 © Fh d 0 m o a © -p O rH C Qt— 1 Oh d W) a d d cd CO O CQ C QO in * i— io o LO rH Distance in feet Bearing • Position C T 3 • N o LO C Q i— 1 to d d o A CD C Q > F h © P FH Oh p *H © o d o CQ pq o P — © d . n © d *o c a •H rH P t> CQ d CQ o © C Q© © o © co tiD d © o CQ o d d d © o d o O © & © P d ■ — *• •H tO d © i— 1 © H Oh g © C Q w- © © o d o o © 4-3 "* © d © in F h to © © d ** a © O fctO O rH P d H Oh© -H CD a d d d © d d O CQ © © O —' CQ PQ o • J—1 o IO I—1 • CQ to 1 —1 to 1 C Q • • N N N o o o LO CQ IO CQ in C Q • CQ . CQ C Q d to O i—1 d ^ O iH •rH p d LO O rH •rH p P © o o A H • NO CD O CQ CQ tO • 3 • N * O © cM CQ •rH F h Oh p «H h* © —« O CO • © to -P s rH CO © • d iz; -> & © 9< a © •H in d 1 — 1 © f> F h • • NO cD ©O C Q © a O r—! Fh © © rH rH • P © d © F H © •* a ud O d i— 1«rH ttOd d d o © o cq O o • LO ** © © g © O i— 1 i—I Oh © in o A E>C Q F h cq d d © rH i— 1 © 53 * o © C Ti p to © & — C Q -—. o> C Q o 1 — 1 * -— vQ to © H O) a © CQ —' 40 -p 0 0 V) O O'-' -P o £H d *0 d CQ 0 ?H 0 * 'd CT> 1 —I ( — l LO cd d > o ~ u & CO to 0 -P 0 *» d •rH -P ts 0 to Fh 0 w 0 i —1 £ 0 Oi —1 0 0 H Ch O W Ei d d 0 o O CO o w o M 0 u 0 d o •H -p 0 O o rd o> —1 1 1 CO rH 41 H d o •H -P cd o o i-H d o *H -P O © CO o d o r—I © P O C QC d © d £ © 1 d P P © © © — ' © *'■ d o^ (S3 o tiD -p d o d © 04 d co d rd © P P ©P •H © O © o

© d O i— 1 -P © i —I © r-i i —I • i— 1r— 1i— 1 © © • o O a MO •rH •H •H CQ P P P ©O CQ d d d d E> © O LO • p 3 ** m w • 0 'd d ^ C Q © © C" ra ,i4 cmo © © © t> > !> S © © Cb g o o d o •rl p o © CO CQ 02 d o p © o o *r! o pq LQ LQ LQ a • rH i—1 © © • O O •H *H “st* -p P CQ d d © © a, at d o o © t> o p * 0K • © ♦ • d i— 1 d tiD O © > © d © 1> w -h M 02 o O d © d •H O LQ o d d C4H« tO P © P •H d •H P o © d * • © i d d © -sF © © w •• • # i —1 S o tiD © © I —1 O d d © *H © i—1 O P & o ttO d d d d d d •rH © d o O d © o CO o ■*■— o © pq d — i i © f> d © P d *H d © rH © © O d o o o p © o d © CQ CQ ,d -p Fh TO d rH © © CQ © d to © H © © O d o o o to cd o ♦ to TO © I—1 © © o d o o o CQ d tO o LQ • -- . p 13 05 ♦ © tO TO <0 d d © © L> © CQ M cd ** *rH o Fh Pi 00 © ♦H P •H p P © TO o© © Fh Fh • * ra © © © a a W i— i o o d I— 1i— i•H CL, «JD ClO tO a © d d TO o o © CQ *-— o o PQ o •pH P © Fh to © g ,— . © © O 1—1 i— 1 tiO a d © o CQ o LQ • L> Fh © P d •rH Fh © P d •rH tO © rH © © o d o o O O r— 1 > d rH © © rH H © -> P o © rH Fh © © a © O rH rH P| £jD £ d © O CQ O t> Fh © P d •H TO © i—1 © © o d o O Kaolin OligocIase-10% Chlorite Muscovite Sericite Precipitates* "cement” ______________ Calcite Minor constituents __________ Magnetite270 Hematite Epidote * Pettijohn, F.J., Sedimentary Hocks, p. 86 (1940). 52 Sample 17. Arkosic sandstone Megascopic description: grained, and bedded* The sandstone is brown, medium The grains are poorly sorted. Brick red, parallel, platy, discontinuous zones about 0.5 millimeters thick (ferruginous clay zones?) are found. Microscopic description: and sub-angular grains. Clastic, poorly sorted, angular The sandstone contains five per cent of igneous rock fragments. These are mainly com­ posed of microlitic feldspars, and possess a felty texture. Stable "primary” minerals* Stable "secondary" minerals* Precipitates* "cement" Quartz-70% Chlorite Calcite 01igoclase-15^ Kaolin Hematite Minor constituents Magnetite­ s'fo Mi cr o c1 ine - 2 0 °/o Perthite-3% Muscovite * Pettijohn, F.J., Sedimentary Rocks, p. 86 (1940). 53 Section III Sample 28. Sandstone (Orthoouartzite) Megascopic description: The sandstone is brown, fine grained, and brecciated. Microscopic description: Clastic, well sorted, angular and sub-angular grains. The spaces between the brecci­ ated fragments are filled with cryptocrystalline quartz, Stable "primary" minerals* Stable "secondary" minerals* Quartz-90% Chlorite Oligoclase -570 Kaolin Biotite Precipitates* "cement" ______________ Calcite Hematite Minor constituents __________ MagnetiteHpidote Zircon * Pettijohn, F.J., Sedimentary Rocks, p. 86 (1940). 54 Section IV Sample 3* Arkosic sandstone Megascopic description: The sandstone is brown, medium grained, bedded, and cut by calcite and quartz veinlets* Microscopic description: Clastic, poorly sorted, angular and sub-angular grains. The sandstone contains about five per cent of igneous rock fragments. These are mainly com­ posed of microlitic feldspars, and possess a felty tex­ ture . Stable "primary” minerals* Stable rse condary” minerals* Precipitates* "cement” Minor cou­ stituents Q.uartz-7 5% Kaolin Calcite-2y0 Zircon Oligoclase-15% Chlorite Hematite Epidote Microcline-3% Sericite Magnetite Orthoclase-£% Muscovite Biotite * Pettijohn, F.J., Sedimentary Hocks, p. 86 (1940). 55 Section V Sample 14. Sandstone (Orthoquartzite) Megascopic description: grained. The sandstone is brown and fine It is bedded and micaceous. Microscopic description: Clastic, well sorted, angular and sub-angular grains. Stable primary" minerals* Stable "secondary" minerals* Q,uartz-85$> Kaolin 01igoclase-10% Chlorite Precipitates* "cement" ______________ Calcite Minor constituents __________ Magnetite2% Hematite Mi cro cl ine - 2fo Muscovite Biotite * Pettijohn, P.J., Sedimentary Rocks, p. 86 (1940). Section VI Sample 3. Sandstone (Orthoquartzite) Megascopic description: The sandstone is brown and fine grained. Microscopic description: Clastic, well sorted, angular and sub-angular grains. Stable "primary” minerals* Stable "secondary" minerals* Precipitates* "cement" Quartz-90% Chlorite Calcite 01igoclase-5% Sericite Hematite Minor constituents Magnetite3°/o Orthoclase Biotite Muscovite * Pettijohn, F.J., Sedimentary Pocks, p. 86 (1940). The Igneous Pebbles Six thin sections of type samples of the igneous pebbles from the coarse conglomerates and the conglomeratic sand­ stones were examined. Pebble 1 . Rhyolite Megascopic description: and aphanitic. Reddish brown, fine grained, Quartz and feldspars are identified with a hand lens. Microscopic description:Holocrystalline, hypautomorphic— granular texture. Primary minerals Secondary minerals Alterations Quartz-35% Hornblende-5$ Sericite 01igoclase-15$ Zircon Kaolinite-10% Perthite-30% Magnetite Hpidote Pebble 2 . Basalt Megascopic description: Greenish gray, very fine grained, and aphanitic. -Microscopic description: Holocrystalline, diabasic texture. Primary minerals Secondary minerals Lab r a dor it e - 60% Magne t it e - lG jo Augite-30^o Kpidote Hornblende Alterations Chlorite-3^ 58 Pebble 3 . Amygdaloidal basalt Megascopic description: Greenish gray, very fine grained, aphanitic, and amygdaloidal. Microscopic description: ture, Holocrystalline, diabasic tex­ Most of the amygdules are filled with crypto­ crystalline quartz. One amygdule is filled with skeleton hematite crystals. Primary minerals Secondary minerals Labradorite-60% Magnetite-5% Augite-30% Kpidote Alterations Chlorite-4% Biotite Apatite Pebble 4 . Trachyte porphyry Megascopic description: and porphyritic. Light brown, very fine grained, The phenocrysts are composed of feldspars. Microscopic description:Hypocrystalline, microlitic tex­ ture, and trachitic structure. The phenocrysts are sub- hedral. Primary minerals Secondary minerals Alterations Quartz-5% Kaolinite Albite-5% Magnetite-2% Chlorite Orthoclase-15% Biotite shreds-3% Phenocrysts: Microlites: Orthoclase(?)-60% Glassy matrix-10% 59 Pebble 5. Trachyte porphyry Megascopic description: and porphyritic. Light brown, very fine grained, The phenocrysts are composed of feldspars. Microscopic description: Hypocrystalline, microlitic tex­ ture, and trachitic structure. The phenocrysts are sub- hedral. Primary minerals Phenocrysts: Albite-3$ 0rthoclase-£0% Secondary minerals Alterations Quartz-5$ Chlorite Magnetite Epidote Microlites: Orthoclase (?) -60fo Glassy matrix-10% Pebble 6 . Rhyolite porphyry Megascopic description: Reddish brown, very fine grained, and porphyritic. The phenocrysts are composed of feld­ spar and quartz. The pebble is fractured. Microscopic description: phenocrysts are subhedral. Hypocrystalline texture. The The fractures in the pebble are filled with cryptocrystalline quartz. 60 Pebble 6 (cont•) Pyj-ffQ-ry minerals Secondary minerals Alterations Phenocrysts: Kaolinite Quartz-5% Perthite-8% Orthoclase-3% Sanidine-2$ Glassy matrix: Feldspars and quartz-82$ 3. General Statement A, The Sandstones The sandstones along all of the sections show a very similar mineralogy and petrography. This is an in­ dication that they have come from the same source or sources. The fine grained sandstones are mostly orthoquartzites, the medium grained are arkosic sandstones, and the coarse grained are arkoses with more than 25 per cent of feldspars. As most of the outcrops are medium grained, it is inferred that the Porcupine Mountains Sandstone in the area studied, is mainly a conglomeratic arkosic sand­ stone with lenses of fine and coarse grained sandstone and arkose. The cement of the orthoquartzites, arkosic sand­ stones, and arkoses is composed of secondary calcite and 61 hematite * The latter is the mineral from which the sandstones derive their characteristic reddish "brown color. B. The Igneous Pebbles A total of one hundred and eighty-eight pebbles were collected from the different outcrops of coarse con­ glomerates and conglomeratic sandstone. These are classified into four main groups: 1. Trachyte porphyry: Seventy-eight pebbles of this group were collected. 2. Rhyolite porphyry: Forty-three pebbles of this group were collected. 3. Basalt: Thirty-four pebbles of this group were collected. 4. Rhyolite: Some are amygdaloidal. Sixteen pebbles of this group were collected. The remaining seventeen pebbles are classified into two additional minor groups: 5. Quartz: Ten pebbles of this group vjere collected. One pebble showed typical agate zoning. 6. Granite: Seven pebbles of this group were collected. One pebble showed gneissic banding. The above described pebbles were found to have a roundness value of .6 to .9, and a sphericity of .67 to .87 (See appendix). The average size of the pebbles is about three inches, but a few boulders of more than one foot in 62 diameter were observed* The pebbles are poorly sorted in their respective zones (Figures 1 and 5). The majority of the pebbles composing the conglom­ erate zones are acidic and intermediate igneous rocks, which can be classified generally as felsites. This is in conformity with the character of most of the pebbles of the Keweenawan conglomerates that outcrop in the Ke­ weenaw Peninsula and along the Black River southwest of the Porcupine Mountains. It is inferred that the felsite pebbles which make up most of the material of the conglomerate zones of the Porcupine Mountains sandstone in the area studied, were derived from the lower Keweenawan rocks* Gordon* be- * Gordon, W.C*, and Lane, A.G., "A Geological Section From Bessemer Down Black River,” Michigan Geological Survey Rept* for 1906, p. 429 (190777 lieves that these rocks were the only possible source of felsites. Other pebbles found, such as granites, quartz, and agates were most probably derived from the pre-Keweenawan rocks, which include the Huronian and the Archeo­ zoic * CORRELATIONS Correlation of the outcrops from one section to another s attempted by the following methods: By lithology: The outcrops in the area are composed of conglomeratic sandstones, sandstones, and thin conglom­ erate zones. The first two lithologic types do not occur in distinct zones, but grade into each other along both the strike and dip, making it impossible to trace any par­ ticular zone from one section to another. The only zones that possess distinct lithology and sharp contacts are those of the coarse conglomerates. Along Sections I, II, III, and IV, all of the conglomerate zones observed were very thin and irregular; but along Section V and VI, rela­ tively large conglomerate zones outcrop in the form of prominent ridges. Along Section V, these outcrop at Loca­ tions 14, 15, and 16; and along Section VI, similar ridges occur at Locations El, E2, and 23 (Map 2). The topographic expression of the area of Sections V and VI indicates that these conglomerate ridges described above are a part of one large conglomerate zone that ex­ tends from Sections V to VI (Plate l). It is not known whether this zone extends to the east, or pinches out some­ where in the area between Sections IV and V. The area west of Section VI was not traversed, and it could not be deter­ mined if the conglomerate zone extends to the west. In an unpublished paper describing outcrops along the 64 Carp and Little Carp Rivers in the Porcupine Mountains, southwest of Section VI, Hornstein* reported the existence Hornstein, O.M., "A Field and Petrographic Study of Some Extrusive and Sedimentary Rocks Along the Carp and Little Carp Rivers in Ontonagon and Gogebic Counties, Michigan." Unpublished Master’s thesis, Department of Geology and Geography, Michigan State College, 1950. of conglomerate zones of very similar character stratigraphically above the Lake Shore Traps formation. It is very probable that one of these zones may be directly re­ lated to the conglomerate zone along Sections V and VI. On a map of the area the regional strike of the Por­ cupine Mountains sandstone was projected from the position of the conglomerate zone of Section V and VI, to the area of the Little Carp and Carp Rivers. At the locations where this projection cuts the two river courses, Hornstein* * Ibid. reported that outcrops of poorly sorted, coarse, felsite conglomerate occur, demonstrating the very probable rela­ tion existing between these zones. It is not within the scope of this investigation to correlate between the area described in this paper, and the area of the Little Carp and Carp Rivers. Nevertheless, it has been shown that relations do exist, both on the basis of lithology and stratigraphic position. More detailed field work in the area between the Little Carp and Carp Rivers and Section YI is, however, necessary before any definite correlations can be established. By the sphericity and roundness of the sand grains and pebbles; Correlation by this method is not possible, be­ cause no distinct zones with a constant sphericity and roundness were noted. On the contrary, variations in sphericity and roundness figures were observed along the strike and dip of the sandstones. This is primarily due to variations in the grain size along the strike and dip. Correlation by this method would have been possible if distinct zones of constant grain sizes occurred. In this case, the sandstone grains would have a constant roundness. This assumption is based on results demonstra­ ted by this investigation; namely, that equal-sized grains of the sandstones in the area studied, possess equal round­ ness. Upon inspection of the roundness and sphericity fig­ ures of the pebbles from the different conglomerate zones, it can be seen that they possess a very similar sphericity and roundness, regardless of the zone from which they came (See appendix). Thus, these figures could not be used as a means of correlating conglomerate zones. 66 CONCLUSION The rooks that outcrop along the six sections traversed are composed mainly of conglomeratic sandstones that exhibit parallel bedding with local cross-bedding (Map 2). Some zones of non-conglomeratic sandstone and coarse conglomerate also occur, probably as lenses. The rocks vary In color from brick red to dark brown, and range in grain size from fine to coarse. They are jointed, possibly faulted, and are cut by irregular veinlets of quartz and calcite. Attempts to correlate the outcrops: 1. By lithology: Correlation was only possible between the conglomerate zones along Sections V and VI (Plate 1). 2. By the sphericity and roundness of the sand grains and pebbles: Correlation was not possible. The sandstones are composed essentially of quartz with minor amounts of oligoclase. Most of the pebbles are composed of intermediate and acidic igneous rocks with minor amounts of basic igneous pebbles. This indicates that the main source of the sediments was an area of outcrops of intermediate and acidic igneous rocks. The most likely area in the vicinity from which these sediments could have been derived is the main Red Rock area in the heart of the Porcupine Mountains. The basalt pebbles found in the conglomerate zones and the conglomeratic sandstones indicate that not all of the sedi­ ments were derived from acidic and intermediate igneous rocks. In the vicinity of the Porcupine Mountains there are large 67 areas where basaltic flows are located*. These are probably * Wright, F.S., and Lane, A.C., "Preliminary Geological Map of the Porcupine Mountains and Vicinity," Michigan Geo­ logical Survey Kept, for 1908, pi. 1 (1909TI the source rocks from which these basic igneous pebbles were derived. The pebbles of the conglomerates and the conglomeratic sandstones are well rounded indicating that they are waterworn. The writer is of the opinion that these sandstones and conglomerates are stream deposits for the following reasons: 1. Thin conglomerate zones are repeated haphazardly through more than 1,500 feet of sandstone. 2. The sandstones are poorly sorted and feldspathic. 3* Ferruginous clay zones are found in the sandstone. 4. Mud cracks are present. 68 -p d o P 05 O Pci 1 P d 05 0 P C D • -P C Q d *(H d O O ■r-o -P 05 P o C D o c{ .-i •H 05 d • t£ 0 C Dd • d •H C D d

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Pi Average roundness 0 d Lithologic type Color Grain size 0 d •rt V d Fh PP 0 P Fh l>s !>> & rd P O P| d Fh Fh O P Ph p d >> Fh o rH 0 tiDP d d O Fh O 0 © P b rP O 0 rH 0 P P 0 Ph Ph 12 d >> Fh b P! Pi d Fh Fh O EH P rH P P Fh 0 £ tiD O •H Fh P P i (D d *rl Vi > 0 Sample number • Fh 0 o Ph P 1 CO £ <£, I ID 0 • d £ W o I tiD O •H Fh id P d tS -p 1 rd d 0 0 *H pt; d d tiDd ■H Fh P tiD -p d § d o p d £ o Fh C Q 1 0 r* ! P Fh •H l>> rH d O Pi t>> Fh © H 1 rsi Fh d 0 p p 0 i —I P Xi 0 Ph Ph O rH 0 tiDP d d O F h O 0 o 0 d d rH 0 0 d 1 CO 00 • p 0 P l co• d 0 0 tlO 0 d rH F hP 0 P t> 0 P F h O O Ph CO* 1 tS 3 0 p 0 Fh >> d Fh P O i 1 Fh 0 > 0 N ID *H 1 0 1 CO• >5 fctO •H d o d 1 Ph 0 d •rH V * o a to F h O 1 ^—i Average sphericity Average sorting Other characteristics 108 0 P 0 F h d Pi 0 d P 0 i 1 Fh O O d © d Pi P, 1 0 C sl p P 0 F h Fh >> d d Fh Ph d O 0 Cr O d d P d © 0 d d h d Di I 1 o rH C O 1 cn C" ♦ 0 d •iH © d •H V V >> F h © >- Fh 0 > > p d d £ tiD O •H Fh rd d p d d £ tiD O •H Fh P P d i d £ d 0 0 *H F H Pd d p 0 P 0 t>^ P v •H i— I d O Pi d v Fh O Eh P i 0 !>> P Fh >5 f>i d d O P d Fh Fh O P P 0 p p p © 0 1 --1 P P 0 0 i 1 P P 0 Ph • • t>s t>> F h d d o p Pi PH « © d *rH V f>. F h 0 o d o d — Ph 109 BIBLIOGRAPHY Books Billings, M.P* Structural Geology, Inc., 1947^ New York: Prentice-Hall, Pettijohn, F.J. Sedimentary Rocks, Book Co., 1940. New York: McGraw-Hill Wahlstron, E.L. Igneous Minerals and Rocks. Wiley & Sons, Inc., 1948. New York: John Reports Butler, B.S., Burbank, W.S., and Collaborators. "The Copper Deposits of Michigan." United States Geological Survey Prof. Paper 144 (19297TGordon, W.C., and Lane, A.C. "A Geological Section From Bessemer Down Black River." Michigan Geological Survey Rept. for 1906, pp. 39^-507, map (1907). Irving, Roland D. "The Copper-Bearing Rocks of Lake Superior." United States Geological Survey Monograph 5 . 464 pages, maps (1883). Lane, A.C. "The Keweenaw Series of Michigan." Michigan Geological Survey, Publication 6 (Geol. Series 4 ), 2 vol., 983 pages, maps (1911). Leith, C.K., Lund, R.J., and Leith, A. "Pre-Cambrian Rocks of the Lake Superior Region." United States Geological Survey Prof. Paper 184, (1935). Mertie, J.B. "Graphic and Mechanical Computation of Thick­ ness of Strata and Distance to a Stratum.” United States Geological Survey Prof. Paper 129-C (1921). Ruthven, A.G. "An Ecological Survey in the Porcupine Mountains and Isle Royale." Michigan Geological Survey Rept. for 1905 (1906). Van Hise, C.R., and Leith, C.K. "The Geology of the Lake Superior Region." United States Geological Survey Monograph 5 2 , 641 pages, maps (l91l). Wright, F.E. "Report of Progress in the Porcupines." Michigan Geological Survey Rept. for 1903, pp. 33-44 (1905). LEGEND EX P L A N A T IO N KEWEENAWAN PORCUPINE MOUNTAINS L.I 5 SANDSTONE 700 Location number T o p og r a p h i c c o n t o u r l ine Intermittent stream 7 Q ar6 O LAKE SHORE TRAPS Basal t i c f l ows HORI ZONTAL SCALE 2 , 0 0 0 F E E T * 1 0 I NCHES BLOCK DIAGRAM OF THE AREA OF SECTIONS V AND VI , SHOWING CORRELATION B E T W E E N CO NGLO M ER A TE V E R T I C A L SCALE THE 50 ZO NE S F E E T « 0*1 I NCHES CONTOUR I N T E R V A L 50 TOPOGRAPHY AND B A S E MAP A F T E R LAKE SHORE TRAPS A F T E R FEET W.A.KELLY R . D . I R V I N G AND F.E. W R I GH T PLATE I HATEM EL-KHALIDI 1950 *43W R44W R 42 W Scale 2,000 1,000 0 2.000 4000 FEET |0 EXPLANATION I 5.7,8,9 S-4, 5, 6 Geologic c o n t a c t Concealed geologic contact S.4 0 Fault Inferred fault Strike and d i p of b e d s Strike and di p o f j o i n t s Strike S . 33.34 12 S.25 S.28,21^X/S.24 S.24 of v e r t i c a l j o i n t s S.21.22.2 3 S.ll S.27 S.I9 * Section ( t r a v e r s e ) n um be r Location number yOS.12,13 9Q*// S.14 15 ^.*^.7 Sample numbe r ie y i f ^ a 4-s Mi ne Mrifi. 7S t a t e J7 highway Intermittent S.1.2 S.1, 2, 3, 4 5 stream OLD CARP L A K E MINE CUYAHOGA MINE T5IN T5IN S. 5.6.7 LONE ISLANOS2s34 S 10,11,12,13 ^ :Li2 j£Z>>S.I4 90 S.15 S.15 / S. 17 5 21,2 y /S 23,2 4 / S.1920 U 3 PROT E R O ZO IC „ \ S 2 >6 ,27,28,29 UPPER K E WE E NAWA N (?) .LI4— S.30,31,32,33,34 S. 3 5,36 .L.I6-S.37, 38,39,40 PORCUPINE MOUNTAINS S A ND S TO N E Conglomeratic sandstone with thin conglomerate zones LOWER K E WE E NA WA N ■L 2 0 S.7,8,9-. L.2I LAKE SHORE TRAPS S. 10, II, 1 2 - V \ S.13.14 Thin bosaltic lava fl ows, a t top amygdaloi dal R 44 W R 43W R42 W MAP OF T HE N O R T H E R N PART OF T HE P OR C UP I N E M O U N T A I N S , O N T O N A G O N COUNT Y, M I C H I G A N BASE MAP AFTER W. A. K E L L Y SHOWING THE AREAL DISTRIBUTION OF THE LAKE SHORE T R A P S , CROSS FAULTS , T H E LOCATION OF T R A V E R S E S L A K E SHORE T R A P S A F T E R ■R-Q IR V IN fi A N D FF W R I f i H T ___ __________________________________________________ . M A P 2 ___________________________________________ AND THE POSITION OF S AMPLES 110 Wright, F.E., and Lane, A.C. "Preliminary Geological Map of the Porcupine Mountains and Vicinity." Michigan Geological Survey Kept, for 1908. plate 1 (1909)V Articles Krumbein, W.C. "Measurement and Geological Significance of Shape and Roundness of Sedimentary Particles." Journal of Sedimentary Petrology, Vol. 11 (1941), pp. 68-69, plate 1, abstract. Rittenhouse, G. "A Visual Method of Estimating TwoDimensional Sphericity." Journal of Sedimentary Petrology, Vol. 13 (1943), pp. 79-81, abstract. Unpublished Material Hornstein, O.M. "A Field and Petrographic Study of Some Extrusive and Sedimentary Rocks Along the Carp and Little Carp Rivers in Ontonagon." Master’s thesis, Department of Geology, Michigan State College (1950). Kelly, W.A. Thaden, R.S. Personal communication. Personal communication.