A field and petrographic study of the sandstones and conglomerates of the Porcupine Mountains, Ontonagon County, Michigan

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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.

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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

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