Geology and Mineral Resources of the Berwick Quadrangle, … · 2012-12-02 · 31 landscape. The major mineral resource in the Berwick area is sand and gravel. 'emendous quantities

Atlas 174c

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK QUADRANGLE, LUZERNE AND COLUMBIA COUNtiES, PENNSYLVANIA

by Jon D. Inners Pennsylvania Geological Survey

PENNSYLVANIA GEOLOGICAL SURVEY FOURTH SERIES HARRISBURG

1978

Atlas 174c

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK QUADRANGLE, LUZERNE AND COLUMBIA COUNtiES, PENNSYLVANIA



1978

Atlas174c

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK QUADRANGLE, LUZERNE AND COLUMBIA COUNTIES, PENNSYLVANIA



1978

..

Atlas 174c

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK QUADRANGLE, LUZERNE AND COLUMBIA COUNTIES, PENNSYLVANIA

by Jo n D. Inn ers Pennsylvania Geological Survey


1978

Copyright 1978 by the

Commonwealth of Pennsylvania

Quotations from this book may be published if credit is given to the Pennsylvania Geological Survey

ADDITIONAL COPIES OF THIS PUBLICA nON MAY BE PURCHASED FROM

STATE BOOK STORE, P. O. BOX 1365 HARRISBURG, PENNSYLVANIA 17125

PREFACE

This report with its accompanying maps describes the nature and distribution of rock formations and surficial deposits in the vicinity of Berwick, northeastern Pennsylvania. The Berwick area has a particularly interesting geologic setting because it lies on the crest of one of the major rock fold structures in the Pennsylvania Appalachians and because it is situated at the edge of the great "terminal moraine," which was deposited by glacial ice and meltwater streams at the end of the Ice Age. Both of these geologic factors have a profound effect on land use, mineral resources, and environmental conditions . Special attention is paid to the influence of geology on groundwater occurrence and quality, cut-slope stability, excavation difficulty, foundation stability, and waste disposal. The vast sand and gravel resources of the area are described, and their geologic significance is explained. The report is designed to have educational as well as practical applications; it is hoped that it will prove not only useful to the professional geologist, engineer, and planner, but also informative to the student and interested layman.

iii

Copyright 1978 by the

Commonwealth of Pennsylvania

Quotations from this book may be published if credit is given to the Pennsylvania Geological Survey

ADDITIONAL COPIES OF THIS PUBLICA nON MAY BE PURCHASED FROM

STATE BOOK STORE, P. O . BOX 1365 HARRISBURG, PENNSYLVANIA 17125

PREFACE

This report with its accompanying maps describes the nature and distribution of rock formations and surficial deposits in the vicinity of Berwick, northeastern Pennsylvania. The Berwick area has a particularly interesting geologic setting because it lies on the crest of one of the major rock fold structures in the Pennsylvania Appalachians and because it is situated at the edge of the great "terminal moraine," which was deposited by glacial ice and meltwater streams at the end of the Ice Age. Both of these geologic factors have a profound effect on land use, mineral resources, and environmental conditions. Special attention is paid to the influence of geology on groundwater occurrence and quality, cut-slope stability, excavation difficulty, foundation stability, and waste disposal. The vast sand and gravel resources of the area are described, and their geologic significance is explained. The report is designed to have educational as well as practical applications; it is hoped that it will prove not only useful to the professional geologist, engineer, and planner, but also informative to the student and interested layman.

iii

CONTENTS

Page

Preface. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. iii Abstract. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1 Introduction. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2

Physical setting. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3 Acknowledgements. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5

Bedrock structure. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 Folds. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 Faults. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7 Clea vage. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 10 Joints. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 11 Fracture traces . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 15

Origin and age of surficial deposits .......... : . . . . . . . . . . . . . . .. 16 Mineral resources. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 22

Sand and gravel ..................................... " 23 Crushed stone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 27 Clay shale. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 28 Uranium ............................................. 28 Particulate coal and coaly shale .......................... " 28

References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 31 Glossary. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 33

ILLUSTRATIONS

FIGURES IN TEXT

Figure 1. Equal-area lower-hemisphere projection of poles to bedding, poles to cleavage, bedding-cleavage intersections, and axes of minor folds . . . . . . . . . . . . . . . . . . . . . . . . . . 6

2. Equal-area lower-hemisphere projection of poles to wedge faults, slickenlines on wedge faults, and slickenlines on bedding .... , .. ... . ... . ... . . ... . ... . .... . .... . 8

3. Equal-area lower-hemisphere projection of poles to joints in the Marcellus, Mahantango, and Harrell Formations. . 12

4. Equal-area lower-hemisphere projection of poles to joints in the Trimmers Rock, Catskill, and Pocono Formations on the north flank of the Berwick anticlinorium. . . . . . . . 13

5. Equal-area lower-hemisphere projection of poles to joints in the Trimmers Rock, Catskill, Spechty Kopf, Pocono, and Mauch Chunk Formations on the south flank of the Berwick anticlinorium. . . . . . . . . . . . . . . . . . . . . . . . . . . 14

CONTENTS

Page

Preface. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. iii Abstract. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1 Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2

Physical setting. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3 Acknowledgements. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5

Bedrock structure. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 Folds. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 Faults. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7 Cleavage . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 10 Joints. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 11 Fracture traces . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 15

Origin and age of surficial deposits .......... .- . . . . . . . . . . . . . . .. 16 Mineral resources. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 22

Sand and gravel ..................................... " 23 Crushed stone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 27 Clay shale. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 28 Uranium ............................................. 28 Particulate coal and coaly shale .......................... " 28

References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 31 Glossary. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 33

ILLUSTRATIONS

FIGURES IN TEXT

Figure 1. Equal-area lower-hemisphere projection of poles to bedding, poles to cleavage, bedding-cleavage intersections, and axes of minor folds . . . . . . . . . . . . . . . . . . . . . . . . . . 6

2. Equal-area lower-hemisphere projection of poles to wedge faults, slickenlines on wedge faults, and slickenlines on bedding .... , .. ... . ... . ... . . ... . ... . .... . .... . 8

3. Equal-area lower-hemisphere projection of poles to joints in the Marcellus, Mahantango, and Harrell Formations. . 12

4. Equal-area lower-hemisphere projection of poles to joints in the Trimmers Rock, Catskill, and Pocono Formations on the north flank of the Berwick anticlinorium. . . . . . . . 13

5. Equal-area lower-hemisphere projection of poles to joints in the Trimmers Rock, Catskill, Spechty Kopf, Pocono, and Mauch Chunk Formations on the south flank of the Berwick anticlinorium. . . . . . . . . . . . . . . . . . . . . . . . . . . 14

'igure 6.

7.

8.

9.

10.

Page

Diagram showing orientation of fracture traces and line-aments. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 15 Diagram showing approximate absolute time at which various surficial processes that left a depositional record were active in the Berwick quadrangle . . . . . . . . . . . . . . . 16 Cumulative curves of grain-size distribution for Wood-fordian sand and gr~iVel samples. . . . . . . . . . . . . . . . . . . . 24 Histograms showing the lithologic composition of Wood-fordian sand and gravel samples. . . . . . . . . . . . . . . . . . . . 25 Cumulative curves of grain-size distribution for Holocene coaly sand and gravel and sand samples. . . . . . . . . . . . . . 30

FIGURES ON PLATE 1

1igures 1-5. Photographs showing-1. Large-scale planar cross beds in greenish-gray medium-grained

sandstone, Sherman Creek Member of the Catskill Formation.

2. Rubble slide in mOderately dipping sandstone, Sherman Creek Member of the Catskill Formation.

3. Calcareous fossil shell (brachiopod) lenses in the middle part of the Trimmers Rock Formation.

4. Siltstone beds, some distinctly graded, in the lower part of the Trimmers Rock Formation.

5. Coarse cleavage in argillaceous, micritic limestone, Tully Member of the Mahantango Formation.

FIGURES ON PLATE 2

'igures 1-7. Photographs showing-1. Convoluted sharpstone colluvium derived from greenish-gray

sandstone and silty clay shale of the Irish Valley Member (Catskill Formation).

2. Typical bedding and sorting variations in Woodfordian out-wash.

3. Cobbly outwash of the 575-foot (175-m) terrace. 4. Cut in a Woodfordian outwash terrace. 5. Inclined bedding in a Woodfordian kame terrace. 6. Torrential bedding in Woodfordian frontal-kame deposits. 7. Large quartz-conglomerate erratic (Pocono or Pottsville For

mation) in Woodfordian ground moraine.

vi

PLATES

(in envelope)

Plate 1. Bedrock geologic map of the Berwick quadrangle, Luzerne and Columbia Counties, Pennsylvania.

2. Surficial geologic map of the Berwick quadrangle, Luzerne and Columbia Counties, Pennsylvania.

TABLES

Page

Table 1. Summary of test results for clay shale samples ... . . . . . .. 29 2. Percent of particulate coal in coaly sand and gravel and

sand samples ................................... 31

vii

'igure 6.

7.

8.

9.

10.

Page

Diagram showing orientation of fracture traces and line-aments. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 15 Diagram showing approximate absolute time at which various surficial processes that left a depositional record were active in the Berwick quadrangle . . . . . . . . . . . . . . . 16 Cumulative curves of grain-size distribution for Wood-fordian sand and gr~lVel samples. . . . . . . . . . . . . . . . . . . . 24 Histograms showing the lithologic composition of Wood-fordian sand and gravel samples. . . . . . . . . . . . . . . . . . . . 25 Cumulative curves of grain-size distribution for Holocene coaly sand and gravel and sand samples . . . . . . . . . . . . . . 30

FIGURES ON PLATE 1

ligures 1-5. Photographs showing-1. Large-scale planar cross beds in greenish-gray medium-grained

sandstone, Sherman Creek Member of the Catskill Formation.

2. Rubble slide in moderately dipping sandstone, Sherman Creek Member of the Catskill Formation.

3. Calcareous fossil shell (brachiopod) lenses in the middle part of the Trimmers Rock Formation.

4. Siltstone beds, some distinctly graded, in the lower part of the Trimmers Rock Formation.

5. Coarse cleavage in argillaceous, micritic limestone, Tully Member of the Mahantango Formation.

FIGURES ON PLATE 2

"igures 1-7. Photographs showing-1. Convoluted sharpstone colluvium derived from greenish-gray

sandstone and silty clay shale of the Irish Valley Member (Catskill Formation).

2. Typical bedding and sorting variations in Woodfordian out-wash.

3. Cobbly outwash of the 575-foot (175-m) terrace. 4. Cut in a Woodfordian outwash terrace. 5. Inclined bedding in a Woodfordian kame terrace. 6. Torrential bedding in Woodfordian frontal-kame deposits. 7. Large quartz-conglomerate erratic (Pocono or Pottsville For

mation) in Woodfordian ground moraine.

vi

PLATES

(in envelope)

Plate I. Bedrock geologic map of the Berwick quadrangle, Luzerne and Columbia Counties, Pennsylvania.

2. Surficial geologic map of the Berwick quadrangle, Luzerne and Columbia Counties, Pennsylvania.

TABLES

Page

Table 1. Summary of test results for clay shale samples . . . . . . . . .. 29 2. Percent of particulate coal in coaly sand and gravel and

sand samples ...................... . ............ 31

vii

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK OUADRANGLE. LUZERNE AND COLUMBIA COUNTIES, PENNSYLVANIA

by Jon D. lnners

ABSTRACT

The Berwick 71f2-minute quadrangle is situated astride the North Branch, Susquehanna River, in the Appalachian Mountain section of the Valley and Ridge physiographic province. Although the topography is mainly controlled by the resistance to erosion of folded sedimentary rocks, depositional landforms related tp glacial and glaciofluvial processes are well developed in the eastern and central parts of the mapped area.

Bedrock formations that underlie the quadrangle range from the Silurian Wills Creek Formation to the Mississippian Mauch Chunk Formation. The rocks are predominantly marine limestones, shales, and siltstones in the lower part of the stratigraphie column (Wills Creek to Trimmers Rock interval) and nonmarine shales, sandstones, and conglomerates in the upper part (Catskill to Mauch Chunk interval).

The dominant bedrock structure in the quadrangle is the Berwick anticlinorium, which plunges gently northeastward and is flanked on the north and south by the Lackawanna and Catawissa-McCauley Mountain synclinoria, respectively .. Fold limbs are composed of long, planar segments separated by sharp hinges. Faults constitute a subordinate part of the structure, although two large south-dipping reverse faults are inferred to displace Silurian and Devonian rocks beneath the terrace gravels at Berwick. Cleavage, which is well developed in argillaceous rocks and also affects limestones, siltstones, and fine-grained sandstones, generally dips steeply to the south and fans across the Berwick anticlinorium. Joints are developed in all lithologies and are generally approximately perpendicular to bedding. Fracture-trace orientations appear to reflect joint trends.

Unconsolidated deposits of Pleistocene and Holocene age comprise numerous surficial units-titls, ice-contact stratified drift, kame-terrace and frontal-kame gravels, outwash, and alluvium-which form a blanket over more than half the mapped area. Deposits of three episodes of continental glaciation can be differentiated on the bases of morphological preservation, depth of weathering, and clast lithology. These glacial events are probably correlative with the Illinoian (oldest), Altonian, and

GEOLOGY AND MINERAL RESOURCES OF THE BERWICK OUADRANGLE. LUZERNE AND COLUMBIA COUNTIES. PENNSYLVANIA

by Jon D. Inners

ABSTRACT

The Berwick 7 1/2-minute quadrangle is situated astride the North Branch, Susquehanna River, in the Appalachian Mountain section of the Valley and Ridge physiographic province. Although the topography is mainly controlled by the resistance to erosion of folded sedimentary rocks, depositional landforms related t9 glacial and glaciofluvial processes are well developed in the eastern and central parts of the mapped area.

Bedrock formations that underlie the quadrangle range from the Silurian Wills Creek Formation to the Mississippian Mauch Chunk Formation. The rocks are predominantly marine limestones, shales, and siltstones in the lower part of the stratigraphie column (Wills Creek to Trimmers Rock interval) and nonmarine shales, sandstones, and conglomerates in the upper part (Catskill to Mauch Chunk interval).

The dominant bedrock structure in the quadrangle is the Berwick anticlinorium, which plunges gently northeastward and is flanked on the north and south by the Lackawanna and Catawissa-McCauley Mountain synclinoria, respectively.. Fold limbs are composed of long, planar segments separated by sharp hinges. Faults constitute a subordinate part of the structure, although two large south-dipping reverse faults are inferred to displace Silurian and Devonian rocks beneath the terrace gravels at Berwick. Cleavage, which is well developed in argillaceous rocks and also affects limestones, siltstones, and fine-grained sandstones, generally dips steeply to the south and fans across the Berwick anticlinorium. Joints are developed in all lithologies and are generally approximately perpendicular to bedding. Fracture-trace orientations appear to reflect joint trends.

Unconsolidated deposits of Pleistocene and Holocene age comprise numerous surficial units-tills, ice-contact stratified drift, kame-terrace and frontal-kame gravels, outwash, and alluvium-which form a blanket over more than half the mapped area. Deposits of three episodes of continental glaciation can be differentiated on the bases of morphological preservation, depth of weathering, and clast lithology. These glacial events are probably correlative with the Illinoian (oldest), Altonian, and

BERWICK QUADRANGLE

oodfordian (youngest) glaciations, which have been recognized in adcent areas of northeastern and north-central Pennsylvania. The Woodrdian (Late Wisconsinan) "terminal" moraine forms a conspicuous belt hummocky, bouldery terrain across the central and northern portions the quadrangle. Rigorous Woodfordian periglacial frost action

'oduced large quantities of colluvium and talus, which were transported )wnslope by gravity-induced mass movement. A widespread mantle of ,Iian silt and fine sand was deposited over the late Woodfordian perigla-31 landscape. The major mineral resource in the Berwick area is sand and gravel. 'emendous quantities of this commodity are available from the glacioflual deposits that border the Susquehanna River. Some potential for the ,mmercial exploitation of clay shale, crushed stone, and particulate 'iver and creek" coal also exists. Although environmental constraints related to geologic conditions in e Berwick area are locally significant, they generally are not serious. 'oundwater supplies adequate for domestic use usually can be obtained )m bedrock at depths of 100 to 200 feet (30 to 60 m), In the area ,rdering the Susquehanna, glaciofluvial gravels serve as a vast storage servoir that supplies large quantities of water to the underlying bedrock rmations. Slope stability in bedrock units is a function of lithology and titude of planar discontinuities. Except for dominantly shaly units, most !drock formations have moderate to high stability in cut slopes greater an 25 degrees, providing that planar discontinuities, such as bedding joints, are not seriously undercut; unconsolidated surficial sediments

e mostly unstable in cuts steeper than 25 degrees. Excavation characristics are mainly related to lithology, but degree of bedding, jointing, ,d cleavage development also plays a significant role; i.e., unconlidated surficial deposits and thin-bedded, cleaved shales can normy be excavated to considerable depth with light to heavy machinery, lereas thick-bedded quartzitic sandstone and conglomerate generally II require blasting. Most bedrock units in the area have suitable founda·n strength for heavy structures; unconsolidated surficial sediments can ually support light structures, but should be investigated for support of !avy structures. Suitability of the various bedrock formations and unconlidated surficial deposits as sites for septic systems and sanitary lands is highly variable and can be properly evaluated only by detailed one investigations.

INTRODUCTION

The Berwick quadrangle encompasses an area of approximately 55.9 uare miles (144.7 km2) in Luzerne and Columbia Counties, northeastern :nnsylvania. The principal center of population is the Borough of Berwick

INTRODUCTION 3

(1970 population, 14,000). Other boroughs and villages of significant size are Nescopeck, Wapwallopen, Foundryville, and Beach Haven. Interstate 80 (the Keystone Shortway) passes through rural countryside in the southern part of the quadrangle, and U. S. Route 11, which follows the north bank of the Susquehanna River, is the main traffic artery serving the more urbanized central portion.

The Berwick area has a diversified economic base. Industries that manufacture food products, cigars, textiles, fabricated metal products, and other durable and nondurable goods are located in Berwick and its immediate vicinity. Rural areas, which constitute about 90 percent of the quadrangle, support a moderately large, but steadily declining, population of grain and dairy farmers. A 2,100-megawatt BWR (boiling water reactor) nuclear power plant, the Susquehanna Steam Electric Station of the Pennsylvania Power and Light Company, is currently being constructed about 2 miles (3.2 km) northeast of Beach Haven, Luzerne County. It is anticipated that this plant will begin generating electricity in the early 1980's.

Previous geologic mapping in the Berwick area has been largely of a reconnaissance nature, although several investigators have made significant contributions to the understanding of the rock formations and unconsolidated surficial deposits. I. C. White (1883) mapped the bedrock geology in the Berwick area as part of an excellent reconnaissance survey of the geology of Wyoming, Lackawanna, Luzerne, Columbia, Montour, and Northumberland Counties. H. C. Lewis (1884) traced the Early Wisconsinan ice front through the area, but mistakenly mapped a large tract of Late Wisconsinan till north of Berwick as part of the "terminal" moraine. Later Frank Leverett (1934) delineated several areas of older drift beyond the Late Wisconsinan glacial border and corrected the mapping of Lewis north of Berwick. L. C. Peltier (1949) discussed the terraces that border the North Branch in the Berwick area as part of a general study of Pleistocene terraces and periglacial phenomena along the entire length of the Susquehanna River. Recent remapping of the deposits associated with the Late Wisconsinan "terminal" moraine complex by O. H. Crowl (personal communication) has been incorporated with slight modification into the present report.

PHYSICAL SETTING

The Berwick quadrangle lies entirely within the Appalachian Mountain section of the Valley and Ridge physiographic province, an area whose distinctive linear topography is the result of differential erosion of folded sedimentary rocks. Thick shale and limestone units are readily eroded and tend to form valleys, whereas dominantly sandstone and conglomerate units, which are more resistant, form rolling uplands and mountain ridges. In the Berwick area, erosion of a major, nearly symmetrical, anticlinal (convexupward) fold in the rock strata has produced similar topography on opposite sides of the Susquehanna River. Steep escarpments with relief of 200 to

BERWICK QUADRANGLE

oodfordian (youngest) glaciations, which have been recognized in adcent areas of northeastern and north-central Pennsylvania. The Woodrdian (Late Wisconsinan) "terminal" moraine forms a conspicuous belt hummocky, bouldery terrain across the central and northern portions the quadrangle. Rigorous Woodfordian periglacial frost action

'oduced large quantities of colluvium and talus, which were transported )wnslope by gravity-induced mass movement. A widespread mantle of ,Iian silt and fine sand was deposited over the late Woodfordian perigla-31 landscape . The major mineral resource in the Berwick area is sand and gravel. 'emendous quantities of this commodity are available from the glacioflual deposits that border the Susquehanna River. Some potential for the ,mmercial exploitation of clay shale, crushed stone, and particulate 'iver and creek" coal also exists. Although environmental constraints related to geologic conditions in e Berwick area are locally significant, they generally are not serious. 'oundwater supplies adequate for domestic use usually can be obtained )m bedrock at depths of 100 to 200 feet (30 to 60 m). In the area Irdering the Susquehanna, glaciofluvial gravels serve as a vast storage servoir that supplies large quantities of water to the underlying bedrock rmations. Slope stability in bedrock units is a function of lithology and titude of planar discontinuities. Except for dominantly shaly units, most !drock formations have moderate to high stability in cut slopes greater an 25 degrees, providing that planar discontinuities, such as bedding jOints, are not seriously undercut; unconsolidated surficial sediments

e mostly unstable in cuts steeper than 25 degrees. Excavation characristics are mainly related to lithology, but degree of bedding, jointing, ,d cleavage development also plays a significant role; i.e., unconlidated surficial deposits and thin-bedded, cleaved shales can normy be excavated to considerable depth with light to heavy machinery, lereas thick-bedded quartzitic sandstone and conglomerate generally II require blasting. Most bedrock units in the area have suitable founda·n strength for heavy structures; unconsolidated surficial sediments can ually support light structures, but should be investigated for support of :avy structures. Suitability of the various bedrock formations and unconlidated surficial deposits as sites for septic systems and sanitary lands is highly variable and can be properly evaluated only by detailed on'e investigations.

INTRODUCTION

The Berwick quadrangle encompasses an area of approximately 55.9 uare miles (144.7 km2) in Luzerne and Columbia Counties, northeastern :nnsylvania. The principal center of population is the Borough of Berwick

INTRODUCTION 3

(1970 population, 14,000). Other boroughs and villages of significant size are Nescopeck, Wapwallopen, Foundryville, and Beach Haven. Interstate 80 (the Keystone Shortway) passes through rural countryside in the southern part of the quadrangle, and U. S. Route 11, which follows the north bank of the Susquehanna River, is the main traffic artery serving the more urbanized central portion.

The Berwick area has a diversified economic base. Industries that manufacture food products, cigars, textiles, fabricated metal products, and other durable and nondurable goods are located in Berwick and its immediate vicinity. Rural areas, which constitute about 90 percent of the quadrangle, support a moderately large, but steadily declining, population of grain and dairy farmers. A 2,100-megawatt BWR (boiling water reactor) nuclear power plant, the Susquehanna Steam Electric Station of the Pennsylvania Power and Light Company, is currently being constructed about 2 miles (3.2 km) northeast of Beach Haven, Luzerne County. It is anticipated that this plant will begin generating electricity in the early 1980's.

Previous geologic mapping in the Berwick area has been largely of a reconnaissance nature, although several investigators have made significant contributions to the understanding of the rock formations and unconsolidated surficial deposits. I. C. White (1883) mapped the bedrock geology in the Berwick area as part of an excellent reconnaissance survey of the geology of Wyoming, Lackawanna, Luzerne, Columbia, Montour, and Northumberland Counties. H. C. Lewis (1884) traced the Early Wisconsinan ice front through the area, but mistakenly mapped a large tract of Late Wisconsinan till north of Berwick as part of the "terminal" moraine. Later Frank Leverett (1934) delineated several areas of older drift beyond the Late Wisconsinan glacial border and corrected the mapping of Lewis north of Berwick. L. C. Peltier (1949) discussed the terraces that border the North Branch in the Berwick area as part of a general study of Pleistocene terraces and periglacial phenomena along the entire length of the Susquehanna River. Recent remapping of the deposits associated with the Late Wisconsinan "terminal" moraine complex by O. H. Crowl (personal communication) has been incorporated with slight modification into the present report.

PHYSICAL SETTING

The Berwick quadrangle lies entirely within the Appalachian Mountain section of the Valley and Ridge physiographic province, an area whose distinctive linear topography is the result of differential erosion of folded sedimentary rocks. Thick shale and limestone units are readily eroded and tend to form valleys, whereas dominantly sandstone and conglomerate units, which are more resistant, form rolling uplands and mountain ridges. In the Berwick area, erosion of a major, nearly symmetrical, anticlinal (convexupward) fold in the rock strata has produced similar topography on opposite sides of the Susquehanna River. Steep escarpments with relief of 200 to

4 . BERWICK QUADRANGLE

300 feet (60 to 90 m), which face each other at a distance of 2.5 miles (4 km) across the central part of the quadrangle, are developed on moderately resistant Upl'er Devonian sandstones and siltstones, which dip to the north on the north side of the Susquehanna and to the south on the south side. Lee and Nescopeck Mountains, each of which has a local relief of 500 to 700 feet (150 to 215 m), are the beveled edges of highly resistant Upper Devonian to Lower Mississippian conglomeratic sandstones; these ridges bear a similar relationship to the structure of the rock strata as those described above.

Although the dominant topographic features of the Berwick quadrangle are related to the resistance to erosion and structural attitude of the bedrock formations, depositional landforms formed by glaciai. and glaciofluvial processes are well developed in the eastern and central portions. The most conspicuous features are the Woodfordian (Late Wisconsinan) "terminal" moraine complex, which trends in a northwest-southeast direction across the central part of the quadrangle, and the Woodfordian glaciofluvial terraces, which border the Susquehanna River.

The Woodfordian "terminal" moraine complex is characterized by relatively subdued depositional topography on the uplands. Kames and kettles provide most of the relief, but locally mounds of till may rise 10 feet (3 m) or more above the surrounding terrain. In several areas the Woodfordian drift border is occupied by thin ground moraine rather than end moraine' (Crowl, 1972, 1975). In the river valley itself the morainal complex is marked by a prominent frontal kame on the south side of the river.

Woodfordian glaciofluvial terraces are prominently displayed along the entire length of the Susquehanna River within the quadrangle. These terraces slope down river about 2 to 6 feet per mile (0.4 to 1.1 m/km), the upper terraces having the steeper gradients (Peltier, 1949). Good examples of terraces can be seen at elevations of 530 and 575 feet (162 and 175 m) at Berwick, 530 and 590 feet (162 and 180 m) at Nescopeck, and 640 feet (195 m) at Beach Haven and Hicks Ferry.

On the uplands west and southwest of the Woodfordian "terminal" moraine, older, pre-Woodfordian glacial deposits are generally thin and rarely exhibit depositional topography. The major exception is along the south side of Lee Mountain in the northwest part of the quadrangle, where gently rolling morainal topography can still be detected on thick, early Wisconsinan (Altonian) drift.

The report area is situated within the drainage basin of the North Branch, Susquehanna River, which follows a generally southwestward course through the northeast and central portions of the quadrangle. Nescopeck Creek, the largest local tributary, enters the Susquehanna at Nescopeck Borough after flowing through upland terrain south of the river in a scenic, deeply incised, meandering valley. The creek breaches Nescopeck Mountain in a narrow, picturesque water gap that is utilized to route the Keystone

BEDROCK STRUCTURE 5

Shortway through the mountain barrier. About 0.6 mile (1 km) west of the gap, southward migration of a large meander bend of Nescopeck Creek has resulted in the erosion of a steep-sided amphitheater into the north slope of the mountain.

ACKNOWLEDGEMENTS

The writer is indebted to many individuals for advice and assistance in the preparation of this report. Field and office discussions with other members of the Survey staff helped to resolve some difficult stratigraphic and structural problems. J. LaRue Smith and David A. Hopkins, at the time undergraduate student interns from Bloomsburg State College, assisted with field mapping in 1976. Detailed geological engineering reports on several earthdam, highway, and bridge construction projects in the Berwick area were provided by Bruce Benton and Louis Kirkaldie, U. S. Department of Agriculture, Soil Conservation Service, and Paul Solomon, Anthony DeAngelo, and Carl Gottshall, Pennsylvania Department of Transportation. Richard H. Howe, PennDOT Bureau of Materials Testing and Research, evaluated several rock samples for suitability as construction aggregate. Richard Wood, Pennsylvania Power and Light Company, granted the author permission to examine rock cuts and excavations at the site of the Susquehanna Steam Electric Station.

Special thanks are due to George H. Crowl of Ohio Wesleyan University, who is largely responsible for mapping the Late Wisconsinan (Woodfordian) morainal deposits.

BEDROCK STRUCTURE

The sedimentary rocks of the Berwick quadrangle were originally deposited as approximately horizontal layers. About 250 million years ago, the rock strata were folded and faulted during the Alleghanian orogeny. All of the structures described below presumably are related to this deforma-tion.

FOLDS

The major structure in the Berwick quadrangle is the Berwick (Montour Ridge) anticlinorium, a moderately complex, first-order fold'" (Nickelsen, 1963) which trends in a northeast-southwest direction across the mapped area. The axis of the fold passes through the center of the quadrangle and plunges N76E at 2 to 4 degrees (Figure 1). In the eastern part of the area, the

*Refer to glossary for explanation of technical terms that are not defined in text.

4 . BERWICK QUADRANGLE

300 feet (60 to 90 m), which face each other at a distance of 2.5 miles (4 km) across the central part of the quadrangle, are developed on moderately resistant Upl'er Devonian sandstones and siltstones, which dip to the north on the north side of the Susquehanna and to the south on the south side. Lee and Nescopeck Mountains, each of which has a local relief of 500 to 700 feet (150 to 215 m), are the beveled edges of highly resistant Upper Devonian to Lower Mississippian conglomeratic sandstones; these ridges bear a similar relationship to the structure of the rock strata as those described above.

Although the dominant topographic features of the Berwick quadrangle are related to the resistance to erosion and structural attitude of the bedrock formations, depositional landforms formed by glaciai. and glaciofluvial processes are well developed in the eastern and central portions. The most conspicuous features are the Woodfordian (Late Wisconsinan) "terminal" moraine complex, which trends in a northwest-southeast direction across the central part of the quadrangle, and the Woodfordian glaciofluvial terraces, which border the Susquehanna River.

The Woodfordian "terminal" moraine complex is characterized by relatively subdued depositional topography on the uplands. Kames and kettles provide most of the relief, but locally mounds of till may rise 10 feet (3 m) or more above the surrounding terrain. In several areas the Woodfordian drift border is occupied by thin ground moraine rather than end moraine' (Crowl, 1972, 1975). In the river valley itself the morainal complex is marked by a prominent frontal kame on the south side of the river.

Woodfordian glaciofluvial terraces are prominently displayed along the entire length of the Susquehanna River within the quadrangle. These terraces slope down river about 2 to 6 feet per mile (0.4 to 1.1 m/km), the upper terraces having the steeper gradients (Peltier, 1949). Good examples of terraces can be seen at elevations of 530 and 575 feet (162 and 175 m) at Berwick, 530 and 590 feet (162 and 180 m) at Nescopeck, and 640 feet (195 m) at Beach Haven and Hicks Ferry.

On the uplands west and southwest of the Woodfordian "terminal" moraine, older, pre-Woodfordian glacial deposits are generally thin and rarely exhibit depositional topography. The major exception is along the south side of Lee Mountain in the northwest part of the quadrangle, where gently rolling morainal topography can still be detected on thick, early Wisconsinan (Altonian) drift.

The report area is situated within the drainage basin of the North Branch, Susquehanna River, which follows a generally southwestward course through the northeast and central portions of the quadrangle. Nescopeck Creek, the largest local tributary, enters the Susquehanna at Nescopeck Borough after flowing through upland terrain south of the river in a scenic, deeply incised, meandering valley. The creek breaches Nescopeck Mountain in a narrow, picturesque water gap that is utilized to route the Keystone

BEDROCK STRUCTURE 5

Shortway through the mountain barrier. About 0.6 mile (1 km) west of the gap, southward migration of a large meander bend of Nescopeck Creek has resulted in the erosion of a steep-sided amphitheater into the north slope of the mountain.

ACKNOWLEDGEMENTS

The writer is indebted to many individuals for advice and assistance in the preparation of this report. Field and office discussions with other members of the Survey staff helped to resolve some difficult stratigraphic and structural problems. J. LaRue Smith and David A. Hopkins, at the time undergraduate student interns from Bloomsburg State College, assisted with field mapping in 1976. Detailed geological engineering reports on several earthdam, highway, and bridge construction projects in the Berwick area were provided by Bruce Benton and Louis Kirkaldie, U. S. Department of Agriculture, Soil Conservation Service, and Paul Solomon, Anthony DeAngelo, and Carl Gottshall, Pennsylvania Department of Transportation. Richard H. Howe, PennDOT Bureau of Materials Testing and Research, evaluated several rock samples for suitability as construction aggregate. Richard Wood, Pennsylvania Power and Light Company, granted the author permission to examine rock cuts and excavations at the site of the Susquehanna Steam Electric Station.

Special thanks are due to George H. Crowl of Ohio Wesleyan University, who is largely responsible for mapping the Late Wisconsinan (Woodfordian) morainal deposits.

BEDROCK STRUCTURE

The sedimentary rocks of the Berwick quadrangle were originally deposited as approximately horizontal layers. About 250 million years ago, the rock strata were folded and faulted during the Alleghanian orogeny. All of the structures described below presumably are related to this deforma-tion.

FOLDS

The major structure in the Berwick quadrangle is the Berwick (Montour Ridge) anticlinorium, a moderately complex, first-order fold'" (Nickelsen, 1963) which trends in a northeast-southwest direction across the mapped area. The axis of the fold passes through the center of the quadrangle and plunges N76E at 2 to 4 degrees (Figure 1). In the eastern part of the area, the

*Refer to glossary for explanation of technical terms that are not defined in text.

BERWICK QUADRANGLE

nain axis is offset slightly to the north by en echelon folding in the Mahan:ango Formation. Apparent structural relief and wavelength of the anti;linorium are 12,000 feet (3,700 m) and 8.2 miles (13 km), respectively. The :old is slightly asymmetrical and cylindrical within the confines of the ~erwick quadrangle. Dips average about 35 degrees on the south limb and to degrees on the north limb; dips greater than 75 degrees that affect more .han 30 feet (10 m) of stratigraphic section were recorded only on the north

~ '1'

. Pole to bedding • Bedding-cleavage intersection , Axis of minor fold

..., Average fold axis

OJ 0

&Po D

a

.. /'.:"

[] Pole to cleavage,north flank of Berwick an1lcllnorlum

o Pole to cleavage,sQuth flank of Berwick anticlinorium

igure 1. Equal-area lower-hemisphere projection of 150 poles to bedding, 87 poles to cleavage, 34 bedding-cleavage intersections, and 24 axes of minor folds.

BEDROCK STRUCTURE 7

side (Figure 1). The limbs of the anticlinorium are composed of planar segments separated by k.ink planes, similar to comparable structures described by Faill (1969, 1973).

The axes of the two other first-order fold structures shown on the bedrock geologic map are conjectural. The axis of the Lackawanna synclinorium almost certainly passes through the northwest corner of the Berwick quadrangle, but its exact location cannot be determined due to lack of outcrop in the glaciated valley of Little Shickshinny Creek. In the extreme southeast corner of the quadrangle, a synclinal axis that can be mapped in the Mauch Chunk Formation along Nescopeck Creek may represent the main axis of the Catawissa-McCauley Mountain synclinorium. Alternatively, this axis may define only one of several en echelon second-order synclines that form the synclinorium in this area.

Exposed second- and third-order folds are developed only in the Marcellus-Mahantango interval and the Mauch Chunk Formation. These folds have wavelengths of 100 to 3,000 feet (30 to 900 m) and very low structural relief, mostly on the order of 50 feet (15 m) or less.

Fourth-order folds with wavelengths of 5 to 50 feet (1.5 to 15 m) are fairly common as drag folds in the Trimmers Rock, Catskill, and Mauch Chunk Formations. These folds plunge gently, both to the northeast and southwest. The average plunge is N74E at 3 degrees (Figure 1).

Although folds in the mapped area were formed mainly by a flexural-slip mechanism, a strong component of flexural-flow folding was also involved (see Oonath and Parker, 1964). Characteristic features of flexural-slip folds that are evident in the Berwick quadrangle are: (1) common occurrence of slickenlines on bedding surfaces; (2) maintenance of roughly the same bedding thickness across the hinges of most fourth-order folds; and (3) frequent occurrence of wedge faults. The prominent cleavage developed in argillaceous rocks and the thickening of beds in the hinges of some fourth-order folds are characteristics of flexural-flow folding.

FAULTS Except for the rather enigmatic Light Street and Berwick faults, which

are covered by terrace gravels in Berwick Borough, faults (Le., fracture~ in the rock along which clearly observable movement has taken place) are minor structural features in the quadrangle. Most are small wedge faults that transect only one or several beds and have 3 feet (1 m) or less displacement. Both the Light Street and Berwick faults are probably south-dipping reverse faults, but their exact geometries are unknown.

Wedge faults lie at small angles (10 to 30 degrees) to bedding; displacement results in lateral shortening and duplication of beds (Cloos, 1961). Those observed in the Berwick quadrangle commonly occur either in the core or on the limbs of drag folds. Small wedge faults not associated with drag folds represent a simple transfer of displacement from one bedding

BERWICK QUADRANGLE

nain axis is offset slightly to the north by en echelon folding in the Mahan:ango Formation. Apparent structural relief and wavelength of the anti:lino~ium. are 12,000 feet (3,700 m) and 8.2 miles (13 km), respectively. The :old IS shghtly asymmetrical and cylindrical within the confines of the ~erwick quadrangle. Dips average about 35 degrees on the south limb and to degrees on the north limb; dips greater than 75 degrees that affect more .han 30 feet (10 m) of stratigraphic section were recorded only on the north

. Pole to bedding • Bedding-cleavage int.rsection x Axis of minor fold *" Average fold axis

'.~.\': , a '.

[] Pol. to cleavage,north flank of Berwick antiClinorium

o Pole to cleavage.south flank of Berwick anticlinorium

igure 1. Equal-area lower-hemisphere projection of 150 poles to bedding, 87 poles to cleavage, 34 bedding-cleavage intersections, and 24 axes of minor folds.

BEDROCK STRUCTURE 7

side (Figure 1). The limbs of the anticlinorium are composed of planar segments separated by ~ink planes, similar to comparable structures described by Faill (1969, 1973).

The axes of the two other first-order fold structures shown on the bedrock geologic map are conjectural. The axis of the Lackawanna synclinorium almost certainly passes through the northwest corner of the Berwick quadrangle, but its exact location cannot be determined due to lack of outcrop in the glaciated vaHey of Little Shickshinny Creek. In the extreme southeast corner of the quadrangle, a synclinal axis that can be mapped in the Mauch Chunk Formation along Nescopeck Creek may represent the main axis of the Catawissa-McCauley Mountain synclinorium. Alternatively, this axis may define only one of several en echelon second-order synclines that form the synclinorium in this area.

Exposed second- and third-order folds are developed only in the Marcellus-Mahantango interval and the Mauch Chunk Formation. These folds have wavelengths of 100 to 3,000 feet (30 to 900 m) and very low structural relief, mostly on the order of 50 feet (15 m) or less.

Fourth-order folds with wavelengths of 5 to 50 feet (1.5 to 15 m) are fairly common as drag folds in the Trimmers Rock, Catskill, and Mauch Chunk Formations. These folds plunge gently, both to the northeast and southwest. The average plunge is N74E at 3 degrees (Figure 1).

Although folds in the mapped area were formed mainly by a flexural-slip mechanism, a strong component of flexural-flow folding was also involved (see Oonath and Parker, 1964). Characteristic features of flexural-slip folds that are evident in the Berwick quadrangle are: (1) common occurrence of slickenlines on bedding surfaces; (2) maintenance of roughly the same bedding thickness across the hinges of most fourth-order folds; and (3) frequent occurrence of wedge faults. The prominent cleavage developed in argillaceous rocks and the thickening of beds in the hinges of some fourth-order folds are characteristics of flexural-flow folding.

FAULTS

Except for the rather enigmatic Light Street and Berwick faults, which are covered by terrace gravels in Berwick Borough, faults (Le., fracture~ in the rock along which clearly observable movement has taken place) are minor structural features in the quadrangle. Most are small wedge faults that transect only one or several beds and have 3 feet (1 m) or less displacement. Both the Light Street and Berwick faults are probably south-dipping reverse faults, but their exact geometries are unknown.

Wedge faults lie at small angles (10 to 30 degrees) to bedding; displacement results in lateral shortening and duplication of beds (Cloos, 1961). Those observed in the Berwick quadrangle commonly occur either in the core or on the limbs of drag folds. Small wedge faults not associated with drag folds represent a simple transfer of displacement from one bedding

BERWICK QUADRANGLE

rface to another. Slickenlines on wedge faults are congruent with those ! bedding surfaces (Figure 2), indicating that the formation of the wedge ults is kinematically related to bedding-slip movements (Faill and Wells, 74). Several large but poorly defined faults of this type apparently occur the wide fault zone in the Mahantango Formation at the Susquehanna !am Electric Station near Beach Haven, Salem Township. Luzerne mnty (41 °05 '32 "N176 °08 '48"W). Other moderately to steeply dipping faults are of local significance. ults with dips in excess of 75 degrees but of unknown relationship to

° .,

" Pole to wed;, fault ° Slickenline on wedge fault • Slickenline on bed din;

., ..

o

'"

m

.. . "" . .,

.0 o~··.o "'- ;... • 0 ..

-. • • 0 iI o· •

·m • ~.!J ~. o •• CJ 0

.- • 0

• 1o

°

• Ol. 8. °

... Pole to great circle defined by all data points

ure 2. Equal-area lower-hemisphere projection of 37 poles to wedge faults, 42 slickenlines on wedge faults, and 65 slickenlines on bedding.

BEDROCK STRUCTURE 9

bedding occur in the fault zone at the Susquehanna Steam Electric Station (R. B. Wells, personal communication). On some of these faults, slickenlines that plunge at very low angles in directions nearly parallel to the fault planes suggest a strong strike-slip component of movement.

The Light Street fault (named for the village of Light Street, located about r mile (1.6 km) northeast of Bloomsburg, Columbia County) is a poorly understood zone of structural and stratigraphic disharmony which has been traced in the Wills Creek-Mahantango interval along the north side of the Berwick anticlinorium for about 20 miles (32 km) west of Berwick. Faulting has apparently caused marked local thinning (or elimination) of the Tonoloway, Keyser, Old Port, and/or Onondaga Formations at various places along the line of outcrop; e.g., along the old railroad on the southwest side of Briar Creek, 0.6 mile (1.0 km) east of Dennis Mills, Columbia County (41 °03 ' 45 "N176 0 18 '27"W, Mifflinville quadrangle). (Stratigraphic thinning of the Old Port-Onondaga interval may also account for some of the apparent loss in section on the north side of the Berwick anticlinorium.) Beds north and south of the fault are often contorted into third- and fourthorder folds and transected by small north-dipping faults which are usually accompanied by brecciation. Such structural features are well exposed in the Mahantango Formation along Pa. Route 93, 0.2 mile (0.3 km) north of Dennis Mills (41 °03'50"NI76°18'54"W, Mifflinville quadrangle) and in the Keyser Formation on the grounds of the Berwick Golf Club, 0.3 mile (0.5 km) southeast of Martzville, Columbia County (41 °03 '57"N/-76°15'42"W, Mifflinville quadrangle).

The geometry of the Light Street fault is ambiguous. It may be (1) a south-dipping reverse fault which locally cuts out part of the stratigraphic section between the Wills Creek and Marcellus; (2) a north-dipping detachment related to a major decollement affecting the same stratigraphic interval in the Parvin Good No. I well, drilled on the crest of the Berwick anticlinorium, 7 miles (11.3 km) northeast of the mapped area (41°07'51"NI75°59'29"W, Wilkes-Barre West quadrangle) (Wood and Bergin, 1970); or (3) a combination of (1) and (2). In the P. Good well about 1,400 feet (425 m) of faulted Marcellus black shale (thickened by the imbrication of several thrust sheets) rests on relatively undisturbed Tonoloway or Upper Wills Creek dolomite and dolomitic limestone. The Keyser, Old Port, and Onondaga are absent (unpublished well log, Pa. Geol. Survey). Because of the surficial cover over the faulted area, no conclusive evidence bearing on the nature of the fault can be cited from the Berwick quadrangle. Therefore, the cross section accompanying the bedrock geologic map (Plate 1) shows the simplest Appalachian style fault mechanism for eliminating section on the north flank of the anticlinorium, i.e., a south-dipping reverse fault. If the Light Street fault is part of the decollement in the P. Good well, the structure on the north flank and at the nose of the Berwick anticlinorium within the quadrangle may be much more complex than interpreted on the cross section.

BERWICK QUADRANGLE

rface to another. Slickenlines on wedge faults are congruent with those l bedding surfaces (Figure 2), indicating that the formation of the wedge ults is kinematically related to bedding-slip movements (Faill and Wells, 74). Several large but poorly defined faults of this type apparently occur the wide fault zone in the Mahantango Formation at the Susquehanna !am Electric Station near Beach Haven, Salem Township, Luzerne )unty (41 °05 '32/1N176°08 '48/1W). Other moderately to steeply dipping faults are of local significance. ults with dips in excess of 75 degrees but of unknown relationship to

• Pole to wedge fault ° Slickenline on wedge fault • Slickenline on bedding

II

°

.. I!I

to . .. II II

II

.0 oo~·.o ac. ~. ..0 • 0

_. .: 0 ~ 0·· II

• Ol.

·11 • ~.!J toe o .." 0 .- • 0

• 1o

8 • °

°

* Pole to great circle defined by all data points

ure 2. Equal-area lower-hemisphere prOjection of 37 poles to wedge faults, 42 slickenlines on wedge faults, and 65 slickenlines on bedding.

BEDROCK STRUCTURE 9

bedding occur in the fault zone at the Susquehanna Steam Electric Station (R. B. Wells, personal communication). On some of these faults, slickenlines that plunge at very low angles in directions nearly parallel to the fault planes suggest a strong strike-slip component of movement.

The Light Street fault (named for the village of Light Street, located about 1 mile (1.6 km) northeast of Bloomsburg, Columbia County) is a poorly understood zone of structural and stratigraphic disharmony which has been traced in the Wills Creek-Mahantango interval along the north side of the Berwick anticlinorium for about 20 miles (32 km) west of Berwick. Faulting has apparently caused marked local thinning (or elimination) of the Tonoloway, Keyser, Old Port, and/or Onondaga Formations at various places along the line of outcrop; e.g., along the old railroad on the southwest side of Briar Creek, 0.6 mile (1.0 km) east of Dennis Mills, Columbia County (41 003 ' 45/1N176 0 18 '27"W, Mifflinville quadrangle). (Stratigraphic thinning of the Old Port-Onondaga interval may also account for some of the apparent loss in section on the north side of the Berwick anticlinorium.) Beds north and south of the fault are often contorted into third- and fourthorder folds and transected by small north-dipping faults which are usually accompanied by brecciation. Such structural features are well exposed in the Mahantango Formation along Pa. Route 93, 0.2 mile (0.3 km) north of Dennis Mills (41 °03 '50 I NI76°18'54"W, Mifflinville quadrangle) and in the Keyser Formation on the grounds of the Berwick Golf Club, 0.3 mile (0.5 km) southeast of Martzville, Columbia County (41 °03 '57 "N/_ 76°1S'42"W, Mifflinville quadrangle).

The geometry of the Light Street fault is ambiguous. It may ?e (1).a south-dipping reverse fault which locally cuts out part of the stratIgraphiC section between the Wills Creek and Marcellus; (2) a north-dipping detachment related to a major decollement affecting the same stratigraphic interval in the Parvin Good No. 1 well, drilled on the crest of the Berwick anticlinorium, 7 miles (11.3 km) northeast of the mapped area (41°07'51 I NI75°59'29"W, Wilkes-Barre West quadrangle) (Wood and Bergin, 1970); or (3) a combination of (1) and (2). In the P. Good well ab~ut 1,400 feet (425 m) of faulted Marcellus black shale (thickened by the Imbrication of several thrust sheets) rests on relatively undisturbed Tonoloway or Upper Wills Creek dolomite and dolomitic limestone. The Keyser, Old Port and Onondaga are absent (unpublished well log, Pa. Geol. Survey). Beca~se of the surficial cover over the faulted area, no conclusive evidence bearing on the nature of the fault can be cited from the Berwick quadrangle. Therefore the cross section accompanying the bedrock geologic map (Plate 1) shows ~he simplest Appalachian style fault mechanism for eliminating section on the north flank of the anticlinorium, i.e., a south-dipping reverse fault. If the Light Street fault is part of the decollement in the P. Good well, the structure on the north flank and at the nose of the Berwick anticlinorium within the quadrangle may be much more complex than interpreted on the cross section.

BERWICK QUADRANGLE

The Berwick fault is a south-dipping reverse fault which repeats the Old Irt and Keyser Formations on the south flank of the anticlinorium. AlJugh the fault is completely concealed by terrace gravels, stratigraphic Jetition is suggested by the fact that a water well drilled by the Berwick 1mber and Supply Company at 329 West Second Street in Berwick l °03 '1O I N/76°14'21"W) bottomed in "flinty limestone" (Old Port?) owman, 1937, p. 100) 1,500 feet (460 m) west of Old Port ledges exposed the bed of the Susquehanna River just downstream from the Berwick:scopeck bridge (41 °03 , 12 "N/76 °13 '57"W). Since other water wells and ucural borings drilled between these two points encountered fine-grained lestone of Keyser-Tonoloway aspect, a fault with the upthrown side to ! south probably exists a short distance south of the lumber company :ll. The Berwick fault extends east-northeastward into an exposed thirdjer anticline in the Marcellus-Mahantango interval.

CLEAVAGE

Cleavage (i.e., closely spaced, parallel partings or planar discontinuities 1t result from structural deformation) is a prominent feature affecting linly argillaceous rocks in the Berwick quadrangle. Two types can be :ognized: (1) a fine, apparently pervasive cleavage developed in clay lie, silty clay shale, and claystone (particularly in the Marcellus, Mahan-19O, and Harrell Formations); and (2) a coarse, nonpervasive cleavage mmonly present in argillaceous limestone in the Tully Member and Old -rt Formation and in silty claystone, siltstone, and very fine to finelined sandstone of the Trimmers Rock, Catskill, and Mauch Chunk Forltions. Fine cleavage is usually expressed by smooth parting separations that are lerally less than Y4 inch (0.6 cm) apart and impart a fissile or "shaly" apHance to the rock. Distinct separations may range up to 2 inches (5 cm) Ht, but the rock between these separations generally shows pervasive avage development. Bedding-cleavage intersections are relatively straight j plunge gently to the northeast and southwest. The average plunge is ~ut N75E at 4 degrees (Figure 1). In the Mahantango Formation, fossils : commonly distorted, with maximum strain parallel to the cleavage. :'::oarse cleavage separations range from Yz inch (1 cm) to about 3 inches 5 cm) and may superficially resemble bedding (Figure 5 on Plate 1). The avage surfaces are usually uneven and form the boundaries of elongate, cleaved lenses of rock, Intersections between bedding and coarse cleavage 'm wavy lineations having an average plunge similar to that formed by : intersection of fine cleavage and bedding. Jenerally both fine and coarse cleavage dip south and fan across the Ber:k anticlinorium (Figure 1), On the north limb the cleavage dip averages Jut 60 degrees and ranges from 45 to 80 degrees (steepening toward the

BEDROCK STRUCTURE 11

axis). In contrast, on the south limb it averages about 80 degrees and ranges from 60 to 90 degrees. Cleavage also fans across third-order folds in the Mauch Chunk Formation south of Nescopeck Mountain. Frequently, coarse cleavage dips 60 to 75 degrees to the northwest on the south-dipping limbs of these folds.

Both fine and coarse cleavage can adversely affect cut-slope stability. Frost riving and chemical weathering along fine cleavage partings cause rapid deterioration of artificial cuts in the Marcellus, Mahantango, and Harrell shales. An instructive example of the influence of coarse-cleavage orientation on cut-slope stability can be observed along Interstate 80, about 1.0 mile (1.6 km) east-southeast of Tank, Black Creek Township, Luzerne County (41 °00 '17 "N/76 °08 '45"W). A steep cut on the westbound lane of the highway nearly coincides with the axial trace of a third-order fold in Mauch Chunk red claystone. At the east end, where cleavage dips steeply to the north into the rock exposure and bedding dips gently to the south into the open cut, much fragmented rock has spalled off onto the catchment area along the roadway. To the west, however, as cleavage fans around the axis of the fold and dips very steeply (88 degrees) to the southeast, considerably less material has broken loose because the cut slope is inclined in the same direction and at a slightly lower angle than the cleavage dip.

JOINTS

Joints (Le., fractures in the rock along which little or no movement has taken place) are developed in all lithologies, but are particularly well expressed in sandstones and siltstones. Strikes of the joints tend to be either roughly parallel to bedding strike (strike joints), approximately normal to bedding strike (dip joints), or markedly oblique to bedding strike (oblique joints). Most strike- and dip-joint planes are oriented approximately perpendicular to bedding planes. This is particularly well shown in the strike joints, which dip south on the north limb of the Berwick anticlinorium (Figure 4) and north on the south limb (Figure 5). Dip joints are approximately vertical on both limbs, whereas oblique joints are often inclined at moderate angles to bedding.

In the Marcellus, Mahantango, and Harrell Formations, joints are often curved and discontinuous. A set of dip joints that strikes about N45W and dips 70SW to SONE (Figure 3) is fairly well developed at most outcrops, however. These joints are generally 1 to 2 feet (0.3 to 0.6 m) apart, with an average spacing of about 1.5 feet (0.5 m). In rare instances, open joints are cemented by veins of calcite.

In formations above the Harrell, the joints, which are generally planar and continuous, can be grouped into several well-defined sets (Figures 4 and 5). They are usually spaced from 6 inches to 3 feet (15 em to 1 m) apart, but range from 1 inch to more than 6 feet (2.5 cm to more than 2 m) apart. The

BERWICK QUADRANGLE

The Berwick fault is a south-dipping reverse fault which repeats the Old ,rt and Keyser Formations on the south flank of the anticlinorium. AlJugh the fault is completely concealed by terrace gravels, stratigraphic Jetition is suggested by the fact that a water well drilled by the Berwick 1mber and Supply Company at 329 West Second Street in Berwick l °03110INI76°14'21"W) bottomed in "flinty limestone" (Old Port?) owman, 1937, p. 100) 1,500 feet (460 m) west of Old Port ledges exposed the bed of the Susquehanna River just downstream from the Berwick:scopeck bridge (41 °03 I 12 "N176 °13 '57"W). Since other water wells and ucural borings drilled between these two points encountered fine-grained lestone of Keyser-Tonoloway aspect, a fault with the upthrown side to ! south probably exists a short distance south of the lumber company H. The Berwick fault extends east-northeastward into an exposed thirdjer anticline in the Marcellus-Mahantango interval.

CLEAVAGE

Cleavage (i.e., closely spaced, parallel partings or planar discontinuities It result from structural deformation) is a prominent feature affecting tinly argillaceous rocks in the Berwick quadrangle. Two types can be :ognized: (1) a fine, apparently pervasive cleavage developed in clay ile, silty clay shale, and claystone (particularly in the Marcellus, Mahan-190, and Harrell Formations); and (2) a coarse, nonpervasive cleavage mmonly present in argillaceous limestone in the Tully Member and Old -rt Formation and in silty claystone, siltstone, and very fine to finelined sandstone of the Trimmers Rock, Catskill, and Mauch Chunk Forltions. Fine cleavage is usually expressed by smooth parting separations that are lerally less than V4 inch (0.6 cm) apart and impart a fissile or "shaly" apuance to the rock. Distinct separations may range up to 2 inches (5 cm) ift, but the rock between these separations generally shows pervasive avage development. Bedding-cleavage intersections are relatively straight j plunge gently to the northeast and southwest. The average plunge is Gut N75E at 4 degrees (Figure 1). In the Mahantango Formation, fossils : commonly distorted, with maximum strain parallel to the cleavage. ::oarse cleavage separations range from Y2 inch (1 cm) to about 3 inches 5 cm) and may superficially resemble bedding (Figure 5 on Plate 1). The avage surfaces are usually uneven and form the boundaries of elongate, cleaved lenses of rock. Intersections between bedding and coarse cleavage 'm wavy lineations having an average plunge similar to that formed by ! intersection of fine cleavage and bedding. Jenerally both fine and coarse cleavage dip south and fan across the Ber:k anticlinorium (Figure 1). On the north limb the cleavage dip averages Jut 60 degrees and ranges from 45 to 80 degrees (steepening toward the


axis). In contrast, on the south limb it averages about 80 degrees and ranges from 60 to 90 degrees. Cleavage also fans across third-order folds in the Mauch Chunk Formation south of Nescopeck Mountain. Frequently, coarse cleavage dips 60 to 75 degrees to the northwest on the south-dipping limbs of these folds.

Both fine and coarse cleavage can adversely affect cut-slope stability. Frost riving and chemical weathering along fine cleavage partings cause rapid deterioration of artificial cuts in the Marcellus, Mahantango, and Harrell shales. An instructive example of the influence of coarse-cleavage orientation on cut-slope stability can be observed along Interstate 80, about 1.0 mile (1.6 km) east-southeast of Tank, Black Creek Township, Luzerne County (41 °00 '17 "N/76 008 '45"W). A steep cut on the westbound lane of the highway nearly coincides with the axial trace of a third-order fold in Mauch Chunk red claystone. At the east end, where cleavage dips steeply to the north into the rock exposure and bedding dips gently to the south into the open cut, much fragmented rock has spalled off onto the catchment area along the roadway. To the west, however, as cleavage fans around the axis of the fold and dips very steeply (88 degrees) to the southeast, considerably less material has broken loose because the cut slope is inclined in the same direction and at a slightly lower angle than the cleavage dip.

JOINTS

Joints (Le., fractures in the rock along which little or no movement has taken place) are developed in all lithologies, but are particularly well expressed in sandstones and siltstones. Strikes of the joints tend to be either roughly parallel to bedding strike (strike joints), approximately normal to bedding strike (dip joints), or markedly oblique to bedding strike (oblique joints). Most strike- and dip-joint planes are oriented approximately perpendicular to bedding planes. This is particularly well shown in the strike joints, which dip south on the north limb of the Berwick anticlinorium (Figure 4) and north on the south limb (Figure 5). Dip joints are approximately vertical on both limbs, whereas oblique joints are often inclined at moderate angles to bedding.

In the Marcellus, Mahantango, and Harrell Formations, joints are often curved and discontinuous. A set of dip joints that strikes about N45W and dips 70SW to 80NE (Figure 3) is fairly well developed at most outcrops, however. These joints are generally 1 to 2 feet (0.3 to 0.6 m) apart, with an average spacing of. about 1.5 feet (0.5 m). In rare instances, open joints are cemented by veins of calcite.

In formations above the Harrell, the joints, which are generally planar and continuous, can be grouped into several well-defined sets (Figures 4 and 5). They are usually spaced from 6 inches to 3 feet (15 em to 1 m) apart, but range from 1 inch to more than 6 feet (2.5 cm to more than 2 m) apart. The

12 BERWICK QUADRANGLE

~.-:-.

. . . . ~~ .. .?~

'd] ~.+

C':G . .

Figure 3. Equal-area lower-hemisphere projection of 192 poles to joints in the Marcellus, Mahantango, and Harrell Formations. Prominent set: B-N I5-25W, 75NE-80SW (dip joints). Contours at I, 2, 4, 8, and 12 percent per I-percent a rea.

.videst spacing is in thick-bedded, coarse-grained to conglomeratic sandstone of the Spechty Kopf and Pocono Formations. Locally, the joint surfaces are covered by small projecting quartz crystals; at anyone outcrop :hese mineralized joints are restricted to one set, which may be either a ;trike, dip, or oblique set.

The orientation of joint and bedding planes is a critical factor in deternining slope stability in rock cuts. Intersection of these planar partings 'orms discrete blocks which may be unstable, particularly if the individual )lanes or their lines of intersection are undercut during excavation. Gravity

,I

Figure 4.


Equal-area lower-hemisphere projection of 278 poles to joints in the Trimmers Rock, Catskill, and Pocono Formations on the north flank of the Berwick anticlinorium (north-dipping beds). Prominent sets: A-N70-85E, 40-60SE (strike joints); B-NI5-30W, 80SW-80NE (dip jOints); C-N40-50E, 70-80SE (oblique joints). Contours at 1, 2, 4, 8, and 12 percent per I-percent area.

stresses may then overcome friction·aJ drag along inclined surfaces, the result being slippage of blocks off the cut slope. Massive failures of this type are most likely to occur where moderate to steeply dipping bedding planes are undercut, as in the channel change of Nescopeck Creek, just north of Interstate 80, Nes.copeck Township, Luzerne County (41 °01 '10"N!-76°10'57"W) (Figure 2 on Plate 1). However, small-scale failures that involve only one or a few joint blocks can occur if any separation or intersec-


~o-:-.o f- ·0_ ° oA ~ _0 ______ ".

Figure 3. Equal-area lower-hemisphere projection of 192 poles to joints in the Marcellus, Mahantango, and Harrell Formations. Prominent set: B-N I5-25W, 75NE-80SW (dip joints). Contours at I, 2, 4, 8, and 12 percent per I-percent a rea.

N'idest spacing is in thick-bedded, coarse-grained to conglomeratic sand-5tone of the Spechty Kopf and Pocono Formations. Locally, the joint surfaces are covered by small projecting quartz crystals; at anyone outcrop :hese mineralized joints are restricted to one set, which may be either a ;trike, dip, or oblique set.

The orientation of joint and bedding planes is a critical factor in deternining slope stability in rock cuts. Intersection of these planar partings 'orms discrete blocks which may be unstable, particularly if the individual )lanes or their lines of intersection are undercut during excavation. Gravity


Figure 4. Equal-area lower-hemisphere projection of 278 poles to joints in the Trimmers Rock, Catskill, and Pocono Formations on the north flank of the Berwick anticlinorium (north-dipping beds). Prominent sets: A-N70-85E, 40-60SE (strike joints); B-NI5-30W, 80SW-80NE (dip jOints); C-N40-50E, 70-80SE (oblique joints). Contours at 1, 2, 4, 8, and 12 percent per I-percent area.

stresses may then overcome frictional drag along inclined surfaces, the result being slippage of blocks off the cut slope. Massive' failures of this type are most likely to occur where moderate to steeply dipping bedding planes are undercut, as in the channel change of Nescopeck Creek, just north of Interstate 80 Nescopeck Township, Luzerne County (41 °01' 10"N/-76°10 '57"W)' (Figu~e 2 on Plate 1). However, small-scale failures that involve only one or a few joint blocks can occur if any separation or intersec-

14

B

BERWICK QUADRANGLE

x Pole to jolntln north- dipping bid, Mauch Chunk Formation o Pole to joint In 5ubhorlzonlal bed, Mauch Chunk Formation • Pole to Joint In south-dipping bed

:igure 5. Equal-area lower-hemisphere projection of 449 poles to jOints in the Trimmers Rock, CatSkill, Spechty Kopf, Pocono, and Mauch Chunk Formations on the south flank of the Berwick anticlinorium. Prominent sets: A-N55-75E, 60-90NW (strike jOints); B-N20-35W, 80NE-80SW (dip joints). Contours at 1,2,4, and 8 percent per I-percent area.

tion "daylights" into an open cut. It should be kept in mind that physical and chemical weathering play an extremely important part in conditioning a slope to fail. A rock slope that appears stable and permanent immediately after it is excavated may deteriorate in a few years to the point that extensive remedial work is necessary.

,1 {


FRACTURE TRACES

Linear features attributable to fractures and visible on aerial photographs and topographic maps are termed fracture traces, or lineaments if more than 1 mile (1.6 km) long (Lattman, 1958). Generally these definitions include only transverse linears (Le., joint traces, etc.), not those parallel to the structural grain (Le., bedding traces). Four types of linear features are commonly plotted as fracture traces or lineaments: (1) abnormally long, straight stream segments; (2) aligned topographic swales or stream segments; (3) soil-tonal alignments in plowed fields; and (4) alignments of evergreen trees in mostly deciduous forests. These features apparently reflect zones of subsurface fracture concentration which have enhanced weathering and groundwat~r ~ov~ment.

Trends of fracture traces in the Berwick quadrangle are shown in Figure 6. Strong trends at azimuths NIO to 15W and N20 to 25W are subparallel to the main dip-joint set that is well developed on both limbs and in the axial portion of the anticlinorium. The trends at N40 to 45E and N60 to 65E can be related to oblique and strike joints, respectively, oriented in these directions. Other trends cannot be readily identified with well-developed joint sets. Lack of a strong linear trend at N75 to 85E, parallel to the strike-joint set that is complementary to the main dip-joint set, is a defect of the method; any fracture traces trending in this direction were assumed by the writer to be bedding traces and were not plotted.

In areas underlain by bedrock formations in which water occurs mainly in secondary fractures rather than in primary pore spaces, a knowledge of the

Figure 6. Diagram showing orientation of 213 fracture traces and lineaments in the Berwick quadrangle (five-degree orientation classes).


x Pole to joint In north- dippinQ bid, Mauch Chunk Formation o Pole 10 jolnlln subhorlzonlal bed, Mauch Chunk Formation • Pole 10 Joint In south-dlppinQ bed

:igure 5. Equal-area lower-hemisphere projection of 449 poles to jOints in the Trimmers Rock, Catskill, Spechty Kopf, Pocono, and Mauch Chunk Formations on the south flank of the Berwick anticlinorium . Prominent sets: A-N55-75E, 60-90NW (strike joints); B-N20-35W, 80NE-80SW (dip joints). Contours at 1,2,4, and 8 percent per I-percent area.

tion "daylights" into an open cut. It should be kept in mind that physical and chemical weathering play an extremely important part in conditioning a 51 ope to fail. A rock slope that appears stable and permanent immediately after it is excavated may deteriorate in a few years to the point that extensive remedial work is necessary.

,1 I


FRACTURE TRACES

Linear features attributable to fractures and visible on aerial photographs and topographic maps are termed fracture traces, or lineaments if more than 1 mile (1.6 km) long (Lattman, 1958), Generally these definitions include only transverse linears (Le., joint traces, etc.), not those parallel to the structural grain (Le., bedding traces). Four types of linear features are commonly plotted as fracture traces or lineaments: (1) abnormally long, straight stream segments; (2) aligned topographic swales or stream segments; (3) soil-tonal alignments in plowed fields; and (4) alignments of evergreen trees in mostly deciduous forests. These features apparently reflect zones of subsurface fracture concentration which have enhanced weathering and groundwat~r qlov~ment.

Trends of fracture traces in the Berwick quadrangle are shown in Figure 6. Strong trends at azimuths NI0 to 15W and N20 to 25W are subparallel to the main dip-joint set that is well developed on both limbs and in the axial portion of the anticlinorium. The trends at N40 to 45E and N60 to 65E can be related to oblique and strike joints, respectively, oriented in these directions. Other trends cannot be readily identified with well-developed joint sets. Lack of a strong linear trend at N75 to 85E, parallel to the strike-joint set that is complementary to the main dip-joint set, is a defect of the method; any fracture traces trending in this direction were assumed by the writer to be bedding traces and were not plotted.

In areas underlain by bedrock formations in which water occurs mainly in secondary fractures rather than in primary pore spaces, a knowledge of the

Figure 6. Diagram showing orientation of 213 fracture traces and lineaments in the Berwick quadrangle (five-degree orientation classes).


location of fracture traces can be a valuable tool for developing groundwater supplies. Recent studies have shown that water wells located on fracture traces, or at the intersection of two or more traces, tend to have higher yields than wells located in inter-trace areas (LaUman and Parizek, 1964; Hollowell and Koester, 1975). Before a well is drilled on a mapped fracture trace, however, an on-site investigation should be conducted in order to determine the reliability of that particular trace and to evaluate other factors that may have a bearing on well yield.

O RIGIN AN D AGE OF SURFICIAL DEPOSITS

The unconsolidated surficial deposits of the Berwick area record mainly Pleistocene and Holocene glacial, glaciofluvial, glaciolacustrine, eolian, periglacial, swamp-related, and fluvial processes that have been active over the past 500,000 years (Figure 7). All but the last of these processes are related to periodic glaciation of the area by continental ice sheets.

Evidence of at least three episodes of glaciation is preserved in the Berwick quadrangle. On the uplands and in some stream valleys in the westcentral and southern part of the area, many thin, discontinuous pods of

G G .. GF - G1F?

525 475 50 500 100 75

103 YEARS B.P.

25 12 0

Pleistocene Holocene Illinoian 3~ Wisconsinan I

: Alton-l :W0o~-I Ian • -fordl

Figure 7. Approximate absolute time at which various surficial processes that left a depositional record were active in the Berwick quadr:angle. G=glacial; GF=glaciofluvial; GFL=glaciofluvial and glaciolacustrine; E =eolian; PG =periglacial; 5R=swamp related; and F=fluvial. (Time scale adapted from Cooke, 1973; Dreimanis and Goldthwait, 1973; and Sevon and others, 1975.)

SURFICIAL DEPOSITS 17

deeply weathered till occur, all of which are probably remnants of an Illinoian drift cover. 1 Compact, reddish-brown, unweathered to slightly ;eathered till of probable Early Wisconsinan (Altonian) age occupies a narrow band south of Lee Mountain. Glacial drift of the "terminal" moraine complex in the northern and east-central parts of the quadrangle is laterally continuous with known Late Wisconsinan (Woodfordian) drift in Monroe, Carbon, and eastern Luzerne Counties, Pennsylvania (Crowl, 1972; Sevon and others, 1975). Periglacial and outwash deposits related to Woodfordian glaciation are widespread to the west of the moraine.

The Illinoian ice sheet advanced into the Berwick area about 500,000 years B.P. (before present) and deposited a blanket of glacial till (Qit) over much of the quadrangle. The abundance of black to light-gray chert, or "flint" (probably derived from the Onondaga Limestone in the Mohawk Valley region of New York), suggests that ice flow was from the northeast.

The maximum extent of the Illinoian glaciation in the North Branch and trunk valleys of the Susquehanna has not yet been clearly delineated. W. D. Sevon (personal communication) has tentatively recognized the boundary of a pre-Woodfordian (here considered Illinoian) ice lobe immediately south of the mapped area at the east end of McCauley Mountain (Nuremberg quadrangle). The ice margin probably trended toward the northeast on the south side of Nescopeck Mountain and crossed the ridge somewhere within the confines of the Berwick quadrangle (see also Williams, 1895, and Leverett, 1934). In the Susquehanna Valley, Hoskins and Sevon (1976) have recognized Illinoian(?) till as far south as West Mahantango Creek, Snyder County, about 46 miles (74 km) southwest of Berwick.

During the wasting of the Illinoian ice, a belt of aligned kame terraces (Qikt) composed of stratified sand and gravel was built up along the north side of the Susquehanna Valley between Salem Creek and East Berwick. The highest preserved portions of these terraces occur on top of bedrock ridges at an elevation of approximately 700 feet (215 m) and appear to slope gently westward. Stagnant ice probably filled the Susquehanna Valley south of the terraces at the time of their deposition. The presence of Illinoian till at elevations lower than 700 feet (215 m) in the valley of Salem Creek and along an unnamed stream 2,500 feet (762 m) to the west indicates that stagnant ice also lay to the north.

During the ensuing Sangamonian Interglacial, the Illinoian deposits were subjected to deep chemical weathering in a climate that was probably considerably milder and wetter than that existing today. The deep soil profile, reddish color, abundant decomposed clasts, and well-developed weathering prisms that are diagnostic of the Illinoian drift are largely the result of Sangamonian alteration.

, The relative age of the thin pre-Woodfordian upland drift is conjectural. Leverett (1934) considered it entirely Illinoian, and Crowl (personal communication) largely concurs. w. D. Sevon (personal communication), however, believes that most of this till is Altonian.


location of fracture traces can be a valuable tool for developing groundwater supplies. Recent studies have shown that water wells located on fracture traces, or at the intersection of two or more traces, tend to have higher yields than wells located in inter-trace areas (LaUman and Parizek, 1964; Hollowell and Koester, 1975). Before a well is drilled on a mapped fracture trace, however, an on-site investigation should be conducted in order to determine the reliability of that particular trace and to evaluate other factors that may have a bearing on well yield.

O RIGIN AN D AGE OF SURFICIAL DEPOSITS

The unconsolidated surficial deposits of the Berwick area record mainly Pleistocene and Holocene glacial, glaciofluvial, glaciolacustrine, eolian, periglacial, swamp-related, and fluvial processes that have been active over the past 500,000 years (Figure 7). All but the last of these processes are related to periodic glaciation of the area by continental ice sheets.

Evidence of at least three episodes of glaciation is preserved in the Berwick quadrangle. On the uplands and in some stream valleys in the westcentral and southern part of the area, many thin, discontinuous pods of

525

G

GF -

500 475

Pleistocene

G

100 75 50 25 12 0

103 YEARS B.P.

H I cene Illinoian ~~ _____ ..!-__ W;:,;.:is~c;.:on:.:.:.:.:.ln:.:.:a:.lin;,.,.......-+ __ _

: Alton-l ;Wood-I Ian • Ifordi

Figure 7. Approximate absolute time at which various surficial processes that left a depositional record were active in the Berwick quadr:angle. G=glacial; GF=glaciofluvial; GFL=glaciofluvial and glaciolacustrine; E =eolian; PG =periglacial; 5R=swamp related; and F=fluvial. (Time scale adapted from Cooke, 1973; Dreimanis and Goldthwait, 1973; and Sevon and others, 1975.)


deeply weathered till occur, all of which are probably remnants of an IlItnoian drift cover. 1 Compact, reddish-brown, unweathered to slightly weathered till of probable Early Wisconsinan (Altonian) age occupies a narrow band south of Lee Mountain. Glacial drift of the "terminal" moraine complex in the northern and east-central parts of the quadrangle is laterally continuous with known Late Wisconsinan (Woodfordian) drift in Monroe, Carbon, and eastern Luzerne Counties, Pennsylvania (Crowl, 1972; Sevon and others, 1975). Periglacial and outwash deposits related to Woodfordian glaciation are widespread to the west of the moraine.

The Illinoian ice sheet advanced into the Berwick area about 500,000 years B.P. (before present) and deposited a blanket of glacial till (Qit) over much of the quadrangle. The abundance of black to light-gray chert, or "flint" (probably derived from the Onondaga Limestone in the Mohawk Valley region of New York), suggests that ice flow was from the northeast.

The maximum extent of the Illinoian glaciation in the North Branch and trunk valleys of the Susquehanna has not yet been clearly delineated. W. D. Sevon (personal communication) has tentatively recognized the boundary of a pre-Woodfordian (here considered Illinoian) ice lobe immediately south of the mapped area at the east end of McCauley Mountain (Nuremberg quadrangle). The ice margin probably trended toward the northeast on the south side of Nescopeck Mountain and crossed the ridge somewhere within the confines of the Berwick quadrangle (see also Williams, 1895, and Leverett, 1934). In the Susquehanna Valley, Hoskins and Sevon (1976) have recognized Illinoian(?) till as far south as West Mahantango Creek, Snyder County, about 46 miles (74 km) southwest of Berwick.

During the wasting of the Illinoian ice, a belt of aligned kame terraces (Qikt) composed of stratified sand and gravel was built up along the north side of the Susquehanna Valley between Salem Creek and East Berwick. The highest preserved portions of these terraces occur on top of bedrock ridges at an elevation of approximately 700 feet (215 m) and appear to slope gently westward. Stagnant ice probably filled the Susquehanna Valley south of the terraces at the time of their deposition. The presence of Illinoian till at elevations lower than 700 feet (215 m) in the valley of Salem Creek and along an unnamed stream 2,500 feet (762 m) to the west indicates that stagnant ice also lay to the north.

During the ensuing Sangamonian Interglacial, the Illinoian deposits were subjected to deep chemical weathering in a climate that was probably considerably milder and wetter than that existing today. The deep soil profile, reddish color, abundant decomposed clasts, and well-developed weathering prisms that are diagnostic of the Illinoian drift are largely the result of Sangamonian alteration.

, The relative age of the thin pre-Woodfordian upland drift is conjectural. Leverett (1934) considered it entirely Illinoian, and Crowl (personal communication) largely concurs. w. D. Sevon (personal communication), however, believes that most of this till is Altonian.

BERWICK QUADRANGLE

The Altonian glaciation, which affected the Berwick area about 50,000

:ars B.P., was apparently much less extensive than the Illinoian. A narrow

,ngue of Altonian ice, 1.0 to 1.5 miles (1.6 to 2.4 km) wide, pushed down

Ie valley south of Lee Mountain and deposited a sheet of till (Qat) which

,cally attains a thickness of 75 feet (23 m). The central and southern por

ons of the quadrangle were apparently ice-free. Sand and gravel deposits

~ao) that form narrow terraces at an elevation of 650 feet (198 m) on the

lst, south, and west sides of the 700-foot (215-m) Illinoian terrace west of

alem Creek and also cap several low bedrock knobs in the same area may

e remnants of an extensive outwash train that choked the Susquehanna

'alley in the late stages of Altonian deglaciation.

The Altonian deposits are not as severely weathered as the Illinoian, but

ley exhibit a significantly deeper soil profile (generally 3 to 5 feet, or I to

.5 m) than Late Wisconsinan deposits (Sevon and others, 1975).

The Late Wisconsinan (Woodfordian) glaciation (about 15,000 to 20,000

ears B.P.) has left a profound imprint on the Berwick quadrangle. Because

Iere has been little erosional modification of its deposits, it is possible to

evelop a much clearer picture of the movement, thickness, and configura

on of the Woodfordian glacier than is possible for the older glaciations.

'he Woodfordian ice sheet advanced across northeastern Pennsylvania to

lard the south-southwest, but was locally deflected to a more southwesterly

irection by the mountain ridges surrounding the Wyoming-Lackawanna

lasin and by similar ridges, such as Nescopeck Mountain, further to the

outh. Glacial grooves and striae on a siltstone ledge 1.15 miles (1.9 km)

lorthwest of Dorrance, Luzerne County (41 °07 '01 "N/76 °01 '26"W, Sy

lertsville quadrangle), trend S42W, whereas fine striations on a ledge of

f1ahantango shale at the Berwick Speedway, about 0.75 mile (1.2 km)

lortheast of Beach Haven (41 °04 '36"N/76°09 '39"W), trend S70W. The

:hange in trend of the striae suggests progressive deflection of ice movement

LIong the topographic grain in the thinner marginal areas of the ice sheet.

~aximum thickness of the ice in the Berwick area is not known, but the fact

hat erratic boulders occur on the crest of Lee Mountain within 2.7 miles

4.3 km) of the Woodfordian border indicates that the ice was at least 500

'eet (152 m) thick at that point. On the south side of the same mountain, the

ce front apparently had a gradient of about 600 feet per mile (115 m/km)

:as computed from the trend of the Woodfordian border on the mountain

ilope). Although the apparent major effects of the Woodfordian glaciation were

lepositional, the abundance of locally derived clasts in the till attests to the

:rosive power of the ice even near its margin. The ragged cliff on Council

::up (Sybertsville quadrangle) just east of Wapwallopen was undoubted

y over steepened by the plucking action of glacial ice, which moved oblique

y across the hilltop and down the valley. Glacial erosion on a smaller scale

s shown by the inclusion of angular blocks of siltstone and sandstone,


plucked from a bedrock ledge, within overlying till in a cut along Salem

Township Route 436, about 2 miles (3.2 km) north-northeast of Beach

Haven (41 °05' 45 "NI76°09 '39"W).

The depositional products of the Woodfordian glaciation consist of end

and ground moraine, ice-contact stratified drift, frontal-kame and kame

terrace gravels, and outwash. Although accumulation of this material oc

curred during advance, still-stand, and retreat of the ice margin, the depos

its associated with the latter two phases are most conspicuous in the Berwick

quadrangle.

Both end and ground moraine are composed predominantly of glacial till.

End moraine (Qwem) formed where the glacial terminus reached a still

stand position marked by equilibrium between advance and wasting. Since

active ice continued to convey debris forward, a massive belt of glacial till,

mixed with considerable stratified sand and gravel deposited by meltwater,

accumulated along the ice margin. The melting of ice blocks buried in the

till produced the hummocky, "knob and kettle" topography that is charac

teristic of end moraine. Ground moraine (Qwgm) accumulated mainly be

hind the still-stand position either by direct deposition beneath active ice or

through the ablation of debris-laden ice during backwasting and downwast

ing. Both types of morainal deposits commonly contain erratic boulders 6

feet (2 m) or more in diameter (Figure 7 on Plate 2).

In the Berwick quadrangle, ground moraine often occurs in front of end

moraine at the drift margin, suggesting that the edge of the active ice during

the late stages of glaciation and early stages of deglaciation was irregular.

Large masses of ice at the margin melted back or stagnated before a signifi

cant amount of debris had accumulated along the actual ice front. Active

ice, however, continued to pile up debris some distance behind the original

margin. The most conspicuous depositional feature of the still-stand and early de

glaciation phases is the large frontal kame (Qwfk) on the south side of the

Susquehanna River, 2.0 miles (3.2 km) east of Nescopeck. The materials in

this deposit, which constitute the coarsest stratified drift in the quadrangle,

may have been deposited in part by streams flowing on top of or within the

glacier. Originally, the frontal kame, which is now restricted to a broad

wedge on the south side of the river, probably extended across the valley to

the low bedrock hills north of Beach Haven. The deposits may even have

partially blocked meltwater discharge down the valley for a brief period (see

below). It is probable that early in the deglaciation phase a zone of ice several

miles or even tens of miles wide became inactive and slowly wasted away.

Within this stagnating ice mass, ice-contact stratified drift (Qwic) was de

posited by meltwater streams in crevasses, tunnels beneath the ice, and de

pressions on top of the ice, forming isolated kames and small kame com

plexes.

BERWICK QUADRANGLE

The Altonian glaciation, which affected the Berwick area about 50.000

:ars B.P., was apparently much less extensive than the Illinoian. A narrow

• ngue of Altonian ice, 1.0 to 1.5 miles (1.6 to 2.4 km) wide, pushed down

Ie valley south of Lee Mountain and deposited a sheet of till (Qat) which

.callyattains a thickness of 75 feet (23 m). The central and southern por

ons of the quadrangle were apparently ice-free. Sand and gravel deposits

~ao) that form narrow terraces at an elevation of 650 feet (198 m) on the

1St, south, and west sides of the 700-foot (215-m) Illinoian terrace west of

alem Creek and also cap several low bedrock knobs in the same area may

e remnants of an extensive outwash train that choked the Susquehanna

"alley in the late stages of Altonian deglaciation.

The Altonian deposits are not as severely weathered as the Illinoian, but

ley exhibit a significantly deeper soil profile (generally 3 to 5 feet, or 1 to

.5 m) than Late Wisconsinan deposits (Sevon and others, 1975).

The Late Wisconsinan (Woodfordian) glaciation (about 15,000 to 20,000

ears B.P.) has left a profound imprint on the Berwick quadrangle. Because

Iere has been little erosional modification of its deposits, it is possible to

eVelop a much clearer picture of the movement, thickness, and configura

on of the Woodfordian glacier than is possible for the older glaciations.

'he Woodfordian ice sheet advanced across northeastern Pennsylvania to

lard the south-southwest, but was locally deflected to a more southwesterly

irection by the mountain ridges surrounding the Wyoming-Lackawanna

lasin and by similar ridges, such as Nescopeck Mountain, further to the

outh. Glacial grooves and striae on a siltstone ledge 1.15 miles (1.9 km)

lorthwest of Dorrance, Luzerne County (41 °07 '01 "N176°01 '26"W, Sy

,ertsville quadrangle), trend S42W, whereas fine striations on a ledge of

.1ahantango shale at the Berwick Speedway, about 0.75 mile (1.2 km)

lortheast of Beach Haven (41 °04 '36"N/76°09 '39"W), trend S70W. The

:bange in trend of the striae suggests progressive deflection of ice movement

Llong the topographic grain in the thinner marginal areas of the ice sheet.

~aximum thickness of the ice in the Berwick area is not known, but the fact

hat erratic boulders occur on the crest of Lee Mountain within 2.7 miles

4.3 km) of the Woodfordian border indicates that the ice was at least 500

'eet (152 m) thick at that point. On the south side of the same mountain, the

ce front apparently had a gradient of about 600 feet per mile (115 m/km)

:as computed from the trend of the Woodfordian border on the mountain

ilope). Although the apparent major effects of the Woodfordian glaciation were

lepositional, the abundance of locally derived clasts in the till attests to the

:rosive power of the ice even near its margin. The ragged cliff on Council

::up (Sybertsville quadrangle) just east of Wapwallopen was undoubted

y over steepened by the plucking action of glacial ice, which moved ob1ique

y across the hilltop and down the valley. Glacial erosion on a smaller scale

s shown by the inclusion of angular blocks of siltstone and sandstone,


plucked from a bedrock ledge, within overlying till in a cut along Salem

Township Route 436, about 2 miles (3.2 km) north-northeast of Beach

Haven (41 °05' 45 "N/76°09 '39"W) .

The depositional products of the Woodfordian glaciation consist of end

and ground moraine, ice-contact stratified drift, frontal-kame and kame

terrace gravels, and outwash. Although accumulation of this material oc

~urred d.uring a~vance, still-stand, and retreat of the ice margin, the depos

Its assOCIated WIth the latter two phases are most conspicuous in the Berwick

quadrangle.

Both end and ground moraine are composed predominantly of glacial till.

End moraine (Qwem) formed where the glacial terminus reached a still

stand position marked by equilibrium between advance and wasting. Since

active ice continued to convey debris forward, a massive belt of glacial till,

mixed with considerable stratified sand and gravel deposited by meltwater,

accumulated along the ice margin. The melting of ice blocks buried in the

till produced the hummocky, "knob and kettle" topography that is charac

t~ristic of ~nd mor~ine. Ground moraine (Qwgm) accumulated mainly be

hmd the stIll-stand position either by direct deposition beneath active ice or

through the ablation of debris-laden ice during backwasting and downwast

ing. Both types of morainal deposits commonly contain erratic boulders 6

feet (2 m) or more in diameter (Figure 7 on Plate 2).

In the Berwick quadrangle, ground moraine often occurs in front of end

moraine at the drift mar~in, suggesting that the edge of the active ice during

the late stages of glaciation and early stages of deglaciation was irregular.

Large masses of ice at the margin melted back or stagnated before a signifi

cant amount of debris had accumulated along the actual ice front. Active

ice, however, continued to pile up debris some distance behind the original

margin.

The most conspicuous depositional feature of the still-stand and early de

glaciation phases is the large frontal kame (Qwfk) on the south side of the

Susquehanna River, 2.0 miles (3.2 km) east of Nescopeck. The materials in

this deposit, which constitute the coarsest stratified drift in the quadrangle,

may have been deposited in part by streams flowing on top of or within the

glacier. Originally, the frontal kame, which is now restricted to a broad

wedge on the south side of the river, probably extended across the valley to

the low bedrock hills north of Beach Haven. The deposits may even have

partially blocked meltwater discharge down the valley for a brief period (see

below). It is probable that early in the deglaciation phase a zone of ice several

miles or even tens of miles wide became inactive and slowly wasted away.

Within this stagnating ice mass, ice-contact stratified drift (Qwic) was de

posited by meltwater streams in crevasses, tunnels beneath the ice, and de

pressions on top of the ice, forming isolated kames and small kame com

plexes.

:0 BERWICK QUADRANGLE

Much of the meltwater that flowed off the end of the wasting glacier was :hanneled down existing valleys, particularly those of the North Branch and Nescopeck Creek. The valleys of Wapwallopen Creek, Little Wapwallopen Creek, and Salem Creek, as well as those of several unnamed streams, also ,erved as meltwater channels. The heads of the meltwater streams are commonly marked by kame complexes along the margin of the Woodfordian moraine; e.g., Salem Creek and two unnamed streams in Nescopeck Township. Not only did the larger meltwater streams deposit much debris in terraces (Qwoa, Qwo) along their length, but locally they were extremely effective agents of erosion. In the valley of Salem Creek between 1100 feet (335 m) and 1,800 feet (550 m) downstream from the old Berwick Water Company dam (41 °05 '49"N176°11'59/1W), several large potholes about 15 feet (4.6 m) in diameter and 10 to 15 feet (3.0 to 4.6 m) deep were scoured out of north-dipping Trimmers Rock siltstone and sandstone in the initial phase of meltwater discharge. The potholes were later breached by downcutting of Salem Creek.

In the stagnation zone, the thinner ice on the highlands melted faster than the thicker valley ice. Toward the end of this period of rapid melting, a long, narrow tongue of stagnant ice that occupied the Wyoming-Lackawanna Valley (ltter, 1938; Peltier, 1949; Hollowell, 1971) extended into the northeastern corner of the mapped area. Meltwater streams flowing in the channel between the stagnant ice tongue and the valley sides built up thick deposits of sand and gravel which, upon final melting of the ice, were left as kame terraces (Qwkt) high above the valley floor. Pitted terraces at 640 feet (195 m) on the west SIde of the Susquehanna, 3.8 miles (6.1 km) northnortheast of Beach Haven, and at 660 feet (201 m) near the confluence of Wapwallopen Creek and the Susquehanna, 0.4 mile (0.6 km) southwest of Wapwallopen, are good examples. The 640-foot (195-m) kame terrace grades downstream into a complex outwash terrace (Qwkto) at approximately the same elevation at Beach Haven and Hicks Ferry. The eastern portion of this outwash terrace may have been deposited against the southern termination of the stagnant ice tongue, as evidenced by bedding inclined about 20 degrees to the northeast in an abandoned gravel pit on the west side of Salem Township Route 450, 2.1 miles (3.4 km) east-northeast of Beach Haven (41 °05 'Ol/1N176°08'25"W).

Irregular melting of the ice tongue and possibly partial damming of the Susquehanna Valley by morainal deposits resulted in meltwater locally being ponded in ice-marginal lakes. Varved silt and clay deposited in such a la.ke is preserved beneath the remnant of a kame terrace at the intersection of U. S. Route 11 and Salem Township Route 346, 3.0 miles (4.8 km) northeast of Beach Haven (41 °06' 19"N/76°08' 18 "W) (Peltier, 1949).

The 640-foot (195-m) outwash terrace at Beach Haven and Hicks Ferry represents the highest of several terraces formed from the tremendous


volumes of outwash gravel that inundated the Susquehanna Valley during the later stages of deglaciation. As the ice front retreated to the northwest, successively lower terraces were formed by erosion and deposition as the river was graded to new ratios of water volume to sediment load in its downstream reaches. The northwest-facing terrace scarps that are prominent on the south side of the river at Nescopeck were probably eroded by downstream migration of the broad arches in the river, which are still evident between Wapwallopen and Lime Ridge (Mifflinville quadrangle).

Remnants of high outwash terraces (Qwo) are also present along Nescopeck Creek. Good examples are preserved at an elevation of about 600 feet (180 m) on both sides of the creek, 0.35 mile (0.56 km) north of Zenith, Luzerne County. The abundance of angular, locally derived sandstone and siltstone clasts in the gravel pit at the mouth of an unnamed tributary on the east side of the creek (Figure 4 on Plate 2) indicates considerable mixing of outwash transported down the Nescopeck with outwash contributed by a meltwater stream that occupied the present tributary valley and headed on the moraine 2.5 miles (4 km) to the east.

A fairly large proglacial lake may have existed at the west end of the Shickshinny Valley during the early stages of deglaciation. In a gravel pit about 800 feet (245 m) west of Legislative Route 19123 at the extreme north edge of the quadrangle in Briar Creek Township, Columbia County (41 °07 '30"NI76°14 '18"W), 10 to 12 feet (3 to 3.7 m) of light-brown ish-red to grayish-red, varved silt and clay underlie about 5 feet (1.5 m) of crossbedded fine pebbly sand and gravel. Varved glaciolacustrine sediments deposited in the same lake as those in the pit may underlie poorly drained, level terrain on the north side of Little Shickshinny Creek to the west.

In late glacial and early postglacial time, before a widespread vegetative cover was established over the landscape, windblown sand and silt (Qem) was deposited over much of the area as a discrete layer overlying all other Pleistocene units. It is especially well developed on and in the vicinity of kame and outwash terraces. The lower 2 to 3 feet (0.6 to 1.0 m) of the eolian mantle usually contains up to 25 percent pebble- and cobble-sized clasts derived from the underlying glacial drift by frost heaving. In a sand pit at the foot of the rock escarpment about 0.25 mile (0.4 km) south of Nescopeck (41 °02'45/1N/76°12'52/1W), eolian sand and silt is interbedded with shale-chip colluvium. Deposition of the eolian mantle was, therefore, coeval with an episode of colluviation at the end of the Woodfordian.

During the advance and wasting of the various ice sheets, the area beyond the ice margin was subject to intense periglacial frost action, resulting in the production of talus (Qt) and shale-chip, sharpstone, and boulder colluvium (Qc, Qbc). These deposits were transported downslope by gravity-induced mass movement, a process that is particularly effective under tundra-like climatic conditions. Although periglacial deposits of pre-Woodfordian age

:0 BERWICK QUADRANGLE

Much of the meltwater that flowed off the end of the wasting glacier was :hanneled down existing valleys, particularly those of the North Branch and Nescopeck Creek. The valleys of Wapwallopen Creek, Little Wapwallopen Creek, and Salem Creek, as well as those of several unnamed streams, also ,erved as meltwater channels. The heads of the meltwater streams are commonly marked by kame complexes along the margin of the Woodfordian moraine; e.g., Salem Creek and two unnamed streams in Nescopeck Township. Not only did the larger meltwater streams deposit much debris in terraces (Qwoa, Qwo) along their length, but locally they were extremely effective agents of erosion. In the valley of Salem Creek between 1100 feet (335 m) and 1,800 feet (550 m) downstream from the old Berwick Water Company dam (41 °05 '49"N/76°11'59/1W), several large potholes about 15 feet (4.6 m) in diameter and 10 to 15 feet (3.0 to 4.6 m) deep were scoured out of north-dipping Trimmers Rock siltstone and sandstone in the initial phase of meltwater discharge. The potholes were later breached by downcutting of Salem Creek.

In the stagnation zone, the thinner ice on the highlands melted faster than the thicker valley ice. Toward the end of this period of rapid melting, a long, narrow tongue of stagnant ice that occupied the Wyoming-Lackawanna Valley (ltter, 1938; Peltier, 1949; Hollowell, 1971) extended into the northeastern corner of the mapped area. Meltwater streams flowing in the channel between the stagnant ice tongue and the valley sides built up thick deposits of sand and gravel which, upon final melting of the ice, were left as kame terraces (Qwkt) high above the valley floor. Pitted terraces at 640 feet (195 m) on the west Side of the Susquehanna, 3.8 miles (6.1 km) northnortheast of Beach Haven, and at 660 feet (201 m) near the confluence of Wapwallopen Creek and the Susquehanna, 0.4 mile (0.6 km) southwest of Wapwallopen, are good examples. The 640-foot (195-m) kame terrace grades downstream into a complex outwash terrace (Qwkto) at approximately the same elevation at Beach Haven and Hicks Ferry. The eastern portion of this outwash terrace may have been deposited against the southern termination of the stagnant ice tongue, as evidenced by bedding inclined about 20 degrees to the northeast in an abandoned gravel pit on the west side of Salem Township Route 450, 2.1 miles (3.4 km) east-northeast of Beach Haven (41 °05 'OI/lN176 °08 '25 "W).

Irregular melting of the ice tongue and possibly partial damming of the Susquehanna Valley by morainal deposits resulted in meltwater locally being ponded in ice-marginal lakes. Varved silt and clay deposited in such a lake is preserved beneath the remnant of a kame terrace at the intersection of u. S. Route 11 and Salem Township Route 346, 3.0 miles (4.8 km) northeast of Beach Haven (41 °06' 19"N176°0S' IS"W) (Peltier, 1949).

The 64O-foot (195-m) outwash terrace at Beach Haven and Hicks Ferry represents the highest of several terraces formed from the tremendous


volumes of outwash gravel that inundated the Susquehanna Valley during the later stages of deglaciation. As the ice front retreated to the northwest s~ccessively lower terraces were formed by erosion and deposition as th; rIver was graded to new ratios of water volume to sediment load in its downstream reaches. The northwest-facing terrace scarps that are prominent on the south side of the river at Nescopeck were probably eroded by downstream migration of the broad arches in the river, which are still evident between Wapwallopen and Lime Ridge (Mifflinville quadrangle).

Remnants of high outwash terraces (Qwo) are also present along Nescopeck Creek. Good examples are preserved at an elevation of about 600 feet (180 m) on both sides of the creek, 0.35 mile (0.56 km) north of Zenith, Luzerne County. The abundance of angular, locally derived sandstone and si1tst~ne clasts in the gravel pit at the mouth of an unnamed tributary on the east SIde of the creek (Figure 4 on Plate 2) indicates considerable mixing of outwash transported down the Nescopeck with outwash contributed by a meltwater stream that occupied the present tributary valley and headed on the moraine 2.5 miles (4 km) to the east.

A fairly large proglacial lake may have existed at the west end of the Shickshinny Valley during the early stages of deglaciation. In a gravel pit about 800 feet (245 m) west of Legislative Route 19123 at the extreme north edge of the quadrangle in Briar Creek Township, Columbia County (41 °07 '30"NI76°14' 18 "W), 10 to 12 feet (3 to 3.7 m) of light-brownish-red to grayish-red, varved silt and clay underlie about 5 feet (1.5 m) of crossbedded fine pebbly sand and gravel. Varved glaciolacustrine sediments deposited in. the same lake as those in the pit may underlie poorly drained, level terram on the north side of Little Shickshinny Creek to the west.

In late glacial and early postglacial time, before a widespread vegetative cover was .established over the landscape, windblown sand and silt (Qem) was deposIted over much of the area as a discrete layer overlying all other Pleistocene units. It is especially well developed on and in the vicinity of kame and outwash terraces. The lower 2 to 3 feet (0.6 to 1.0 m) of the eolian mantle usually contains up to 25 percent pebble- and cobble-sized clasts derived from the underlying glacial drift by frost heaving. In a sand pit at the foot of the rock escarpment about 0.25 mile (0.4 km) south of Nescopeck (4P02'45/1N/76°12'52/1W), eolian sand and silt is interbedded with shale-chip colluvium. Deposition of the eolian mantle was therefore coeval with an episode of colluviation at the end of the Woodfo;dian. '

During the advance and wasting of the various ice sheets, the area beyond the ice margin was subject to intense periglacial frost action, resulting in the production of talus (Qt) and shale-chip, sharpstone, and boulder colluvium (Qc, Qbc). These ~eposits were transported downslope by gravity-induced mass movement, a process that is particularly effective under tundra-like climatic conditions. Although periglacial deposits of pre-Woodfordian age

BERWICK QUADRANGLE

lve been recognized in nearby areas (Bucek, 1975), all such deposits

apped for this report formed during or subsequent to the Woodfordian

aciation. The probable presence of permafrost in the Woodfordian peri

adal environment is suggested by convolutions in some colluvial masses

ligure 1 on Plate 2). Mixing of colluviated Illinoian and Altonian drift

ith the bedrock-derived colluvium (Qct) and removal of the older drift

leets from many upland areas were both brought about by intense Wood

lrdian frost action. Formation of colluvium and talus in Holocene (Re

!nt) times is probably a minor phenomenon, although some talus and col

lvium is undoubtedly still forming at the base of large cliffs, such as those

n the northwest face of Council Cup and in the meander scar on Nesco

eck Mountain. Deposition of swamp deposits (Qs) in closed and poorly drained depres

ons (many of which are kettle holes that mark the sites of melted ice

locks) has continued relatively uninterrupted from late glacial times down

) the present day. The largest swampy tracts occur in the northern part of

ile quadrangle in an area of thick Altonian and Woodfordian drift along

h.e south side of Lee Mountain. A few of these swamps may contain a si!

tificant thickness of peat beneath the surface layer of humus and gray or

.anicmud. The major Hol~cene natural landscape modifications involve the deposi

ion of sandy and gravelly alluvium (Qal) along the Susquehanna River,

~escopeck Creek, Black Creek, Wapwallopen Creek, and many smaller

treams. Nearly all of this material is deposited during the waning stages of

easonal or storm-related floods. Much of the alluvium in Nescopeck Creek

md the Susquehanna River comprises material reworked from Woodfor

lian outwash deposits. Along the minor streams the alluvium is mixed with

:olluvium (Qac), a large percentage of which represents relict periglacial de

)osits. Fan-shaped concentrations of alluvial materials (Qf) have formed

IVhere tributary streams empty into their master streams and where intermit

.ent rills having steep gradients debouch onto the terrace~ bordering the

;usquehanna. The largest alluvial fan in the quadrangle is situated at the

nouth of Nescopeck Creek across the Susquehanna River from Berwick.

MINERAL RESOURCES

The major economic mineral resource of the Berwick area is sand and

~ravel, vast quantities of which are available for exploitation in the frontal

{arne, kame terraces, and outwash terraces along the Susquehanna River.

Jther materials with a significant potential for commercial development are

:rushed stone and clay shale. Speculative and probable subeconomic re

;ources include uranium, particulate coal, and coaly shale.

MINERAL RESOURCES 23

SAND AND GRAVEL

Geologic factors that determine the economic value of sand and gravel re

sources are: (1) thickness and areal extent of the deposits; (2) grain size,

sorting of the clasts, and shape of the constituent particles; (3) lithology of

the clasts within the various size fractions; and (4) weathering of the clasts.

In many instances, however, strictly economic factors, such as distance of

transport and current land use patterns, are the most important considera

tions. The best sand and gravel resources in the Berwick quadrangle are those in

the Woodfordian frontal kame, kame terraces, and outwash terraces that

border the Susquehanna River. These deposits are often 50 to 75 feet (15 to

23 m) thick and locally exceed 150 feet (46 m) in thickness. Although their

volume is enormous, amounting to several hundred million cubic yards, a

large percentage of the deposits is currently unavailable for exploitation be

cause of residential, commercial, industrial, and agricultural development.

The terrace and frontal-kame deposits exhibit great variation in grain size

and sorting from bed to bed (Figures 2, 3, and 6 on Plate 2). Beds range

from poorly sorted, cobbly and bouldery gravel to moderately well sorted,

fine to coarse sand. Typical grain-size distributions for some coarse pebbly

sands and gravels are shown in Figure 8, A-F. Althougli boulders 5 feet (1.5

m) or more in diameter are frequent in the frontal kame east of Nescopeck,

the largest clasts normally encountered in the terraces are about 1 foot (0.3

m) in diameter. Clasts larger than 4 inches (10 cm) must be crushed in order

to meet size and grading requirements for even the coarsest aggregate (No.

4) approved by the Pennsylvania Department of Transportation. Most of

the pebbles, cobbles, and boulders are subrounded to rounded; subangular

boulders occur in the frontal kame.

Lithology of the particles in the terrac.e and frontal-kame deposits is di

verse and reflects the great variety of rock types encountered by the Wood

fordian glacier on its passage from eastern Canada and northern New York

southward into northeastern Pennsylvania (Figure 9, A-C). About 95 per

cent of the pebble-sized and coarser clasts are derived from bedrock forma

tions that crop out either within the mapped area or in the Wyoming-Lacka

wanna Basin immediately to the northeast. Exotic pebbles, including granit

ic gneiss from the Adirondack Mountains and dark-gray chert from the Mo

hawk Valley region, constitute a small but conspicuous portion of the

clasts. Although claystone and clay shale may locally compose up to 25 per

cent of the pebbles, the great majority are of durable lithologies, such as

well-cemented sandstone. Whereas . the medium to coarse sand fraction is

composed generally of more than 75 percent rock fragments, the fine and

medium sand fraction is 40 to 65 percent vein quartz.

Weathering is generally not a significant factor affecting the suitability of

the Woodfordian terrace and frontal-kame gravels for construction mate-

BERWICK QUADRANGLE

lve been recognized in nearby areas (Bucek, 1975), all such deposits

apped for this report formed during or subsequent to the Woodfordian

aciation. The probable presence of permafrost in the Woodfordian peri

acial environment is suggested by convolutions in some colluvial masses

ligure 1 on Plate 2). Mixing of colluviated Illinoian and Altonian drift

ith the bedrock-derived colluvium (Qct) and removal of the older drift

leets from many upland areas were both brought about by intense Wood

lrdian frost action. Formation of colluvium and talus in Holocene (Re

:nt) times is probably a minor phenomenon, although some talus and col

lvium is undoubtedly still forming at the base of large cliffs, such as those

n the northwest face of Council Cup and in -the meander scar on Nesco

eck Mountain. Deposition of swamp deposits (Qs) in closed and poorly drained depres

ons (many of which are kettle holes that mark the sites of melted ice

locks) has continued relatively uninterrupted from late glacial times down

) the present day. The largest swampy tracts occur in the northern part of

ae quadrangle in an area of thick Altonian and Woodfordian drift along

ne south side of Lee Mountain. A few of these swamps may contain a sig

Jficant thickness of peat beneath the surface layer of humus and gray or

.anicmud. The major Hol~cene natural landscape modifications involve the deposi

ion of sandy and gravelly alluvium (Qal) along the Susquehanna River,

~escopeck Creek, Black Creek, Wapwallopen Creek, and many smaller

treams. Nearly all of this material is deposited during the waning stages of

easonal or storm-related floods. Much of the alluvium in Nescopeck Creek

md the Susquehanna River comprises material reworked from Woodfor

lian outwash deposits. Along the minor streams the alluvium is mixed with

:olluvium (Qac), a large percentage of which represents relict periglacial de

)osits. Fan-shaped concentrations of alluvial materials (Qf) have formed

",here tributary streams empty into their master streams and where intermit

.ent rills having steep gradients debouch onto the terrace:) bordering the

~usquehanna. The largest alluvial fan in the quadrangle is situated at the

nouth of Nescopeck Creek across the Susquehanna River from Berwick.

MINERAL RESOURCES

The major economic mineral resource of the Berwick area is sand and

~ravel, vast quantities of which are available for exploitation in the frontal

(arne, kame terraces, and outwash terraces along the Susquehanna River.

)ther materials with a significant potential for commercial development are

;rushed stone and clay shale. Speculative and probable subeconomic re

iources include uranium, particulate coal, and coaly shale.


SAND AND GRAVEL

Geologic factors that determine the economic value of sand and gravel re

sou~ces are: (1) thickness and areal extent of the deposits; (2) grain size,

sortmg of the clasts, and shape of the constituent particles; (3) lithology of

the clasts. within the various size fractions; and (4) weathering of the clasts.

In many mstances, however, strictly economic factors, such as distance of

t~ansport and current land use patterns, are the most important considera

tIOns.

The best sand and gravel resources in the Berwick quadrangle are those in

the Woodfordian frontal kame, kame terraces, and outwash terraces that

border t~e Susquehanna River. These deposits are often 50 to 75 feet (15 to

23 m) thick and locally exceed 150 feet (46 m) in thickness. Although their

volume is enormous, amounting to several hundred million cubic yards, a

large percentage of the deposits is currently unavailable for exploitation be

cause of residential, commercial, industrial. and agricultural development.

The terrace and frontal-kame deposits exhibit great variation in grain size

and sorting from bed to bed (Figures 2, 3, and 6 on Plate 2). Beds range

from poorly sorted, cobbly and bouldery gravel to moderately well sorted,

fine to coarse sand. Typical grain-size distributions for some coarse pebbly

sands and gravels are shown in Figure 8, A-F. Although boulders 5 feet (1.5

m) or more in diameter are frequent in the frontal kame east of Nescopeck,

the "ar~est clasts normally encountered in the terraces are about 1 foot (0.3

m) 10 diameter. Clasts larger than 4 inches (10 cm) must be crushed in order

to meet size and grading requirements for even the coarsest aggregate (No.

4) apPT.oved by the Pennsylvania Department of Transportation. Most of

the pebbles, cobbles, and boulders are subrounded to rounded; subangular

boulders occur in the frontal kame.

Lithology of the particles in the terrac.e and frontal-kame deposits is di

verse and reflects the great variety of rock types encountered by the Wood

fordian glacier on its passage from eastern Canada and northern New York

southward into northeastern Pennsylvania (Figure 9, A-C). About 95 per

cent of the pebble-sized and coarser clasts are derived from bedrock forma

tions that crop out either within the mapped area or in the Wyoming-Lacka

~ann~ Basin immedi~tely to the northeast. Exotic pebbles, including granit

IC gneISS from the AdIrondack Mountains and dark-gray chert from the Mo

hawk Valley region, constitute a small but conspicuous portion of the

clasts. Although claystone and clay shale may locally compose up to 25 per

cent of the pebbles, the great majority are of durable lithologies, such as

well-cemented sandstone. Whereas . the medium to coarse sand fraction is

composed generally of more than 75 percent rock fragments, the fine and

medium sand fraction is 40 to 65 percent vein quartz.

Weathering is generally not a significant factor affecting the suitability of

the Woodfordian terrace and frontal-kame gravels for construction mate-

~

'"

BERWICK QUADRANGLE

o~I·~~ __________ ~ ______ L-__ ~ __ ~~--~--~----~--~---J 100 10 4 2 o.!! .2~0 .125 .062

gure

Groin slze,ln millim-elers

B. Cumulative curves of grain-size distribution for Woodfordian sand and gravel samples from the Berwick quadrangle. A. Woodfordian frontal kame (Qwfk), Honey Hole Sand and Gravel Company pit, south side of Susquehanna River along Legislative Route 655, 2 miles (3.2 km) east of Nescopeck (41 °03' 39"N/76° 10' 29"W); B. Woodfordian outwast-l (Qwo), at greenhouse on Salem Township Route 430, East Berwick (41°03'51"N/76°12'44"W); C. Woodfordian outwash (Qwo), Line Street near Salem Township Elementary School, East Berwick (41 °03'52"N/76°13'27"W); D. Woodfordian kame terrace and outwash, undivided (Qwkto), west side of Salem Township Route 450, 2.1 miles (3.4 km) eastnortheast of Beach Haven (41°05'01"NI76°0B'25"W); E. Woodfordian kame terrace and outwash, undivided (Qwkto), at township building on west side of Salem Township Route 450, 2 miles (3.2 km) east-northeast of Beach Haven (41004'54"N/7600B'27"W); F. Woodfordian kame terrace (Qwkt), west side of U.S. Route II, 3.8 miles (6.1 km) northeast of Beach Haven (41 °07 '06"N/76°0B'21 "W); G. Woodfordian ice-contact stratified drift (Qwic), east side of Pa. Route 239, O.B mile (1.3 km) northeast of Briggsville (41 °03 '04"N/76°07' 43"W); and H. Woodfordian 'outwash (Qwo), west side of Nescopeck Township Route 376, 0.35 mile (0.56 km) north of Zenith (41 °02 '05"N/76°11 '2B"W).

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B. Cumulative curves of grain-size distribution for Woodfordian sand and gravel samples from the Berwick quadrangle. A. Woodfordian frontal kame (Qwfk), Honey Hole Sand and Gravel Company pit, south side of Susquehanna River along Legislative Route 655, 2 miles (3.2 km) east of Nescopeck (41 0 03'39"N/76 0 10'29"W); B. Woodfordian outwast-l (Qwo), at greenhouse on Salem Township Route 430, East Berwick (41°03'51"N/76°12'44"W); C. Woodfordian outwash (Qwo), Line Street near Salem Township Elementary School, East Berwick (41 °03'52"N/76°13'27"W); D. Woodfordian kame terrace and outwash, undivided (Qwkto), west side of Salem Township Route 450, 2.1 miles (3.4 km) eastnortheast of Beach Haven (41°05'01"NI76°0B'25"W); E. Woodfordian kame terrace and outwash, undivided (Qwkto), at township building on west side of Salem Township Route 450, 2 miles (3.2 km) east-northeast of Beach Haven (41 0 04'54"N/76°08'27"W); F. Woodfordian kame terrace (Qwkt), west side of U.S. Route 11, 3.B miles (6.1 km) northeast of Beach Haven (41 °07 '06"N/76°0B'21 "W); G. Woodfordian ice-contact stratified drift (Qwic), east side of Pa. Route 239, O.B mile (1.3 km) northeast of Briggsville (41 0 03'04"N/76°07'43"W); and H. Woodfordian 'outwash (Qwo), west side of Nescopeck Township Route 376, 0.35 mile (0.56 km) north of Zenith (41 °02 '05"N/76°11 '2B"W).

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rials. Soft, weathered siltstone and sandstone, much of which may be derived from older glacial drift, usually constitutes less than 10 percent of the pebbles. However ~ local concentrations of weathered clasts may render portions of some deposits unsuitable for specific uses that require a high-grade aggregate.

Two commercial operators are active in the frontal kame east of Nescopeck. Both Honey Hole Sand and Gravel Company (40°03 '39"N/-76°10 '36"W) and Hess Brothers, Inc. (41 0 03 '39"NI76°09'33"W) produce Type A gravel and fine aggregate for use in highway and other construction. Large, recoverable reserves of sand and gravel remain in this deposit. Many other pits were formerly worked for sand and gravel in the kame and outwash terraces on the north side of the river. Material is still periodically taken out of these old pits.

Local supplies of sand and gravel can be obtained from the many small Woodfordian ice-contact stratified-drift deposits that occur on the uplands and along the Susquehanna River and from the remnants of Woodfordian outwash terraces along Nescopeck Creek. Individually, these deposits are mostly less than 25 feet (7.6 m) thick and contain less than 500,000 cubic yards (380,000 m 3

) of material. Bed-to-bed grain-size and -sorting variations are comparable to those of the outwash and terrace deposits (Figure 8, G-H), but angular clasts are much more common. The ice-contact stratified-drift deposits (especially those on the uplands) and the terrace remnants on Nescopeck Creek generally exhibit less variety in pebble lithology than the Susquehanna terraces and frontal kame (Figure 9, D-F). Both samples D and F show a preponderance of olive-gray, very fine grained sandstone, siltstone, and silty clay shale derived from the underlying Irish Valiey Member of the Catskill Formation and the nearby Trimmers Rock Formation. The abundance of rather soft, platy siltstone, silty clay shale, and claystone in some of these deposits may make them unsuitable for uses that require a durable aggregate composed of equidimensional fragments. Weathered clasts are relatively uncommon, however .

CRUSHED STONE

Siliceous siltstone, sandstone, and shale in the lower half of the Trimmers Rock Formation were formerly quarried for crushed stone at "Crusher Hill," 1.9 miles (3 km) north of Wapwallopen, Conyngham Township, Luzerne County (41 °06 '09 "N176 °07 '32"W). Tests performed on samples from this quarry by the Pennsylvania Department of Transportation, Bureau of Materials Testing and Research, indicate that the material has good to very good durability and might serve satisfactorily as granular subgrade and subbase for highway construction (R. H. Howe, personal communication). Siltstone and very fine to fine-grained sandstone from the upper part of the quarry would probably have high skid resistance if the material was found otherwise suitable as an aggregate for bituminous pavements.

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rials. Soft, weathered siltstone and sandstone, much of which may be derived from older glacial drift, usually constitutes less than 10 percent of the pebbles. However ~ local concentrations of weathered clasts may render portions of some deposits unsuitable for specific uses that require a high-grade aggregate.

Two commercial operators are active in the frontal kame east of Nescopeck. Both Honey Hole Sand and Gravel Company (40°03 '39"N/-76°10 '36"W) and Hess Brothers, Inc. (41 °03 '39"NI76°09'33"W) produce Type A gravel and fine aggregate for use in highway and other construction . Large, recoverable reserves of sand and gravel remain in this deposit. Many other pits were formerly worked for sand and gravel in the kame and outwash terraces on the north side of the river. Material is still periodically taken out of these old pits .

Local supplies of sand and gravel can be obtained from the many small Woodfordian ice-contact stratified-drift deposits that occur on the uplands and along the Susquehanna River and from the remnants of Woodfordian outwash terraces along Nescopeck Creek. Individually, these deposits are mostly less than 25 feet (7.6 m) thick and contain less than 500,000 cubic yards (380,000 m3

) of material. Bed-to-bed grain-size and -sorting variations are comparable to those of the outwash and terrace deposits (Figure 8, G-H), but angular clasts are much more common. The ice-contact stratified-drift deposits (especially those on the uplands) and the terrace remnants on Nescopeck Creek generally exhibit less variety in pebble lithology than the Susquehanna terraces and frontal kame (Figure 9, D-F). Both samples D and F show a preponderance of olive-gray, very fine grained sandstone, siltstone, and silty clay shale derived from the underlying Irish Valiey Member of the Catskill Formation and the nearby Trimmers Rock Formation. The abundance of rather soft, platy siltstone, silty clay shale, and claystone in some of these deposits may make them unsuitable for uses that require a durable aggregate composed of equidimensional fragments. Weathered clasts are relatively uncommon, however.

CRUSHED STONE

Siliceous siltstone, sandstone, and shale in the lower half of the Trimmers Rock Formation were formerly quarried for crushed stone at "Crusher Hill," 1.9 miles (3 km) north of Wapwallopen, Conyngham Township, Luzerne County (41 °06'09"N/76°07 '32"W). Tests performed on samples from this quarry by the Pennsylvania Department of Transportation, Bureau of Materials Testing and Research, indicate that the material has good to very good durability and might serve satisfactorily as granular subgrade and subbase for highway construction (R. H. Howe, personal communication). Siltstone and very fine to fine-grained sandstone from the upper part of the quarry would probably have high skid resistance if the material was found otherwise suitable as an aggregate for bituminous pavements.


CLAY SHALE

Clay shales and claystones constitute nearly the entire thickness of the Mahantango and Harrell Formations and a large part of the Catskill and Mauch Chunk Formations. Four samples were collected from several stratigraphic horizons in the Mahantango and Harrell and were tested by the U. S. Bureau of Mines for their ceramic and other properties (Table 1). All four samples showed good potential for use in structural clay products, such as building and facing brick. The two samples from the Mahantango Formation also exhibited marginal potential for expanded lightweight aggregate.

URANIUM

Although the writer found no uranium mineralization within the Berwick quadrangle, ample territory for exploration is provided by the large area underlain by the potentially uraniferous Catskill Formation (McCauley, 1961). Two prospect adits, which were probably excavated about twenty years ago in search of uranium, are located on the south slope of Lee Mountain at the north edge of the quadrangle (41 °07 '24"N176°10'54"W). The adits, one of which is at least 30 feet (9 m) deep, are cut into alluvial finingupward cycles at the base of the Duncannon Member. McCauley (1961) reported uranium mineralization from a somewhat lower stratigraphic horizon in the same outcrop belt of the Catskill Formation at a prospect pit about 1.1 miles (1.8 km) southwest of Orangeville, Columbia County (41 °04' 12"N176 °26'OO"W, Bloomsburg quadrangle). Continued interest in the uranium potential of the Berwick-Bloomsburg area is indicated by the fact that private concerns conducted an airborne radiometric survey in the spring of 1977.

PARTICULATE COAL AND COALY SHALE

Particulate anthracite coal is abundant in Holocene alluvial deposits along both Nescopeck Creek and the Susquehanna River, and also occurs to a lesser extent in Woodfordian kame-terrace and outwash sands. The coalrich beds are predominantly moderately well sorted, fine- to mediumgrained, quartz-lithic sands, with the coal fraction generally somewhat coarser than the modal grain size (Figure 10; Table 2). Coal in the Woodfordian sands is usually decomposed to soft, black powder, whereas Holocene particulate coal is quite fresh.

The wealth of particulate coal in the Holocene alluvium of the Berwick area is the result of the coal mining activity in the Northern and Eastern Middle Anthracite fields during the last century and a half (Sisler and others, 1928). In the middle and late 1800's tremendous amounts of fine-

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29 28 BERWICK QUADRANGLE

CLAY SHALE

Clay shales and claystones constitute nearly the entire thickness of the

Mahantango and Harrell Formations and a large part of the Catskill and

Mauch Chunk Formations. Four sampleS were collected from several strati

graphic horizons in the Mahantango and Harrell and were tested by the

U. S. Bureau of Mines for their ceramic and other properties (Table 1). All

four samples showed good potential for use in structural clay products,

such as building and facing brick. The two samples from the Mahantango

Formation also exhibited marginal potential for expanded lightweight

aggregate.

URANIUM

Although the writer found no uranium mineralization within the Berwick

quadrangle, ample territory for exploration is provided by the large area

underlain by the potentially uraniferous Catskill Formation (McCauley,

1961). Two prospect adits, which were probably excavated about twenty

years ago in search of uranium, are located on the south slope of Lee Moun

tain at the north edge of the quadrangle (41 °07'24"N176°10'54"W). The

adits, one of which is at least 30 feet (9 m) deep, are cut into alluvial fining

upward cycles at the base of the Duncannon Member. McCauley (1961) re

ported uranium mineralization from a somewhat lower stratigraphic hori

zon in the same outcrop belt of the Catskill Formation at a prospect pit

about 1.1 miles (1.8 km) southwest of Orangeville, Columbia County

(41 °04'12"N176°26'OO"W, Bloomsburg quadrangle). Continued interest in

the uranium potential of the Berwick-Bloomsburg area is indicated by the

fact that private concerns conducted an airborne radiometric survey in the

spring of 1977.

PARTICULATE COAL AND COALY SHALE

Particulate anthracite coal is abundant in Holocene alluvial deposits

along both Nescopeck Creek and the Susquehanna River, and also occurs to

a lesser extent in Woodfordian kame-terrace and outwash sands. The coal

rich beds are predominantly moderately well sorted, fine- to medium

grained, quartz-lithic sands, with the coal fraction generally somewhat

coarser than the modal grain size (Figure 10; Table 2). Coal in the Wood

fordian sands is usually decomposed to soft, black powder, whereas Holo

cene particulate coal is quite fresh.

The wealth of particulate coal in the Holocene alluvium of the Berwick

area is the result of the coal mining activity in the Northern and Eastern

Middle Anthracite fields during the last century and a half (Sisler and

others, 1928). In the middle and late 1800's tremendous amounts of fine-

MINERAL RESOURCES

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29


Donath, F. ,A., and Parker, R. B. (1964), Folds and folding, Geo!. Soc. America Bull., v. 75, p.45-62.

Dreimanis, A., and Goldtflwait, R. P. (1973), Wisconsin glaciation in the Huron, Erie, and Ontario lobes, in Black, R. F. , Goldthwait, R. P ., and William, H . B., eds . , The Wisconsinan Stage, Geo!. Soc. America Memoir 136, p. 71-106.

Faill, R. T. (1969), Kink band structures in the Valley and Ridge province, central Pennsylvania, Geo!. Soc. America Bull., v. 80, p. 2539-2550.

_____ (1973), Kink band folding, Valley and Ridge province, Pennsylvania, Geo!. Soc. America Bull ., v. 84, p. 1289-1314.

Faill , R. T., and WeBs, R. B. (1974), Geology and mineral resources of the Millerstown quadrangle, Perry, Juniata, and Snyder Counties, Pennsylvania, Pa. Geo!. Survey, 4th ser., Atlas 136.

Fleuty, M. J. (1975), Slickensides and slickenlines, Geo!. Mag., v. 112, p. 319-322. Glaeser, J. D. (1974), Upper Devonian stratigraphy and sedimentary environments in north

eastern Pennsylvania, Pa. Geol . Survey, 4th ser. , Gen. Geology Rept. 63. Hollowell, J . R. (1971), Hydrology of the Pleistocene sediments in the Wyoming Valley, Lu

.. erne County, Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 28. Hollowell, J. R., and Koester, H. E. (1975), Ground-water resources of Lackawanna County,

Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 41. Hoskins, D. M., and Sevon, W. D. (1976), New Illinoian till(?) locality and river terraces in the

Millersburg area, Susquehanna River Valley, Pennsylvania [abs.], Geo!. Soc. America Abs. with Programs, v. 8, no. 2, p . 200.

!tter, H. A. (1938), The geomorphology of the Wyoming-Lackawanna region, Pa. Geo!. Survey, 4th ser., Gen. Geology Rept. 9.

Lattman, L. H. (1958), Technique of mapping geologic fracture traces and lineaments on aerialphotographs, Photogramm. Eng., v. 24, p. 568-576.

Lattman, L. H., and Parizek, R. R. (1964), Relationship between fracture traces and the occurrence of ground water in carbonate rocks, Jour. Hydrology, v. 2, p. 73-91.

Leverett, F. (1934), Glacial deposits outside the Wisconsin Terminal Moraine, Pa. Geo!. Survey, 4th ser. , Gen. Geology Rept. 7.

Lewis, H. C. (1884), Report on the terminal moraine in Pennsylvania and western New York, Pa. Geol. Survey, 2nd ser., Rept. Z.

Lowman, S. W. (1937), Ground water in northeastern Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 4.

McCauley, J . F. (1961), Uranium in Pennsylvania, Pa. Geo!. Survey, 4th ser., Mineral Resource Rept. 43.

Newport, T. G. (1977), Summary of ground-water resources of Luzerne County, Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 40.

Nickelsen, R. P. (1963), Fold patterns and continuous deformation mechanisms of central Pennsylvania folded Appalachians, in Tectonics and Cambro-Ordovician stratigraphy in the central Appalachians of Pennsylvania, Pittsburgh Geo!. Soc. and Appalachian Geo!. Soc., field conf. guidebook, Pittsburgh Pa., Pittsburgh Geo!. Soc., p. 13-29.

Peltier, L. C. (1949), Pleistocene terraces of the Susquehanna River, Pennsylvania, Pa. Geol. Survey, 4th ser., Gen. Geology Rept. 23.

Sevon, W. D. (1969), The Pocono Formation in northeastern Pennsylvania, Guidebook, 34th Annual Field Conr. Pa. Geologists, Pa. Geo!. Survey.

Sevon, W. D., Crowl, O. H., and Berg, T. M. (1975), The Late Wisconsinan drift border in northeastern Pennsylvania, Guidebook, 40th Annual Field Conf. Pa. Geologists, Pa. Geo!. Survey.

Sisler, J. D., Fraser, T., and Ashmead, D. C. (1928), Anthracite culm and silt, Pa. Geo!. Sur. vey, 4th ser., Mineral Resource Rept. 12.

GLOSSARY 33

Walker, R. G . , and Harms, J . C. (1971), The "Catskill Delta, " aprograding muddy shoreline in central Pennsylvania, Jour. Geology, v. 79, p. 381-399.

White, I. C. (1883), Geology of the Susquehanna River region in the six counties of Wyoming, Lackawanna, Luzerne, Columbia, Montour, and Northumberland, Pa. Geo!. Survey, 2nd ser., Rept. G7.

Williams, E. H. (1895), Notes on the southern ice limit in eastern Pennsylvania, Am. Jour. ScL , 3rd ser. , v. 49, p. 174-185.

Wood, G. H., Jr., and Bergin, M. J. (1970), Structural controls of the anthracite region, Pennsylvania, in Fisher, G. W., and others, eds., Studies of Appalachian geology, central and southern, New York, Interscience, p. 141-160.

GLOSSARY

Clast. An individual grain or fragment of a sediment or rock. Decollement. A detachment surface upon which large-scale sliding has

taken place as a result of crustal deformation; strata above and below the detachment exhibit independent styles of deformation.

Efflorescent. Pertaining to minerals that change to powder from loss of water of crystallization.

Eolian. Pertaining to the wind and to sediments that are transported and deposited by the wind.

First-order fold, second-, third-, fourth-order folds. A classification of folds of different sizes by wavelength. First-order-6 to 12 miles (10 to 20 km); second-order-0.6 to 6 miles (1 to 10 km); third-order-66 feet to 0.6 mile (20 m to 1 km); fourth-order-8 inches to 66 feet (20 em to 20m).

Glaciofluvial. Pertaining to meltwater streams flowing from glaciers or to the deposits made by such streams.

Glaciolacustrine. Pertaining to lakes that are marginal to glaciers and to the sediments deposited in such lakes.

Intertidal. Pertaining to the seashore area between mean high tide and mean low tide.

Orogeny. A period· of mountain building; also the process by which the structures (folds, faults, etc.) within mountain areas are formed.

Periglacial. Pertaining to the region or environment adjacent to a glacier. Pickeringite. Hydrated magnesium aluminum sulfate, MgAI2-

(SO.).·22H20; characterized by its astringent taste. Prograding shoreline. A shoreline that is being built outward into the sea by

deposition and accumulation of sediment. Slickenside. A polished and smoothly striated surface that results from fric

tion along a fault plane. Individual striations on this surface are called slickenlines (Fleuty, 1975).

Subtidal. Pertaining to shallow sea bottoms that lie between mean low tide and a depth of about 300 feet (90 m).


Donath, F. ,A., and Parker, R. B. (1964), Folds and folding, Geo!. Soc. America Bull., v. 75, p.45-62.

Dreimanis, A., and Goldtflwait, R. P. (1973), Wisconsin glaciation in the Huron, Erie, and Ontario lobes, in Black, R. F., Goldthwait, R. P., and William, H. B., eds., The Wisconsinan Stage, Geo!. Soc. America Memoir 136, p. 71-106.

Faill, R. T. (1969), Kink band structures in the Valley and Ridge province, central Pennsylvania, Geo!. Soc. America Bull., v. 80, p. 2539-2550.

_____ (1973), Kink band folding, Valley and Ridge province, Pennsylvania, Geo!. Soc. America Bull., v. 84, p. 1289-1314.

Faill, R. T., and Wells, R. B. (1974), Geology and mineral resources of the Millerstown quadrangle, Perry, Juniata, and Snyder Counties, Pennsylvania, Pa. Geo!. Survey, 4th ser., Atlas 136.

Fleuty, M. J. (1975), Slickensides and slickenlines, Geo!. Mag., v.ll2,p. 319-322. Glaeser, 1. D. (1974), Upper Devonian stratigraphy and sedimentary environments in north

eastern Pennsylvania, Pa. Geol. Survey, 4th ser., Gen. Geology Rept. 63. Hollowell, J. R. (1971), Hydrology of the Pleistocene sediments in the Wyoming Valley, Lu

zerne County, Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 28. Hollowell, J. R., and Koester, H. E. (1975), Ground-water resources of Lackawanna County,

Pennsylvania, Pa. Geo!. Survey, 4th ser., Watef' Resource Rept. 41. Hoskins, D. M., and Sevon, W. D. (1976), New Illinoian till(?) locality and river terraces in the

Millersburg area, Susquehanna River Valley, Pennsylvania [abs.], Geo!. Soc. America Abs. with Programs, v. 8, no. 2, p. 200.

liter, H. A. (1938), The geomorphology of the Wyoming-Lackawanna region, Pa. Geo!. Survey, 4th ser., Gen. Geology Rept. 9.

Lattman, L. H. (1958), Technique of mapping geologic fracture traces and lineaments on aerialphotographs, Photogramrn. Eng., v. 24, p. 568-576.

Lattman, L. H., and Parizek, R. R. (1964), Relationship between fracture traces and the occurrence of ground water in carbonate rocks, Jour. Hydrology, v. 2, p. 73-91.

Leverett, F. (1934), Glacial deposits outside the Wisconsin Terminal Moraine, Pa. Geo!. Survey, 4th ser., Gen. Geology Rept. 7.

Lewis, H. C. (1884), Report on the terminal moraine in Pennsylvania and western New York, Pa. Geo!. Survey, 2nd ser., Rept. Z.

Lowman, S. W. (1937), Ground water in northeastern Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 4.

McCauley, J. F. (1961), Uranium in Pennsylvania, Pa. Geo!. Survey, 4th seL, Mineral Resource Rept. 43.

Newport, T. G. (1977), Summary of ground-water resources of Luzerne County, Pennsylvania, Pa. Geo!. Survey, 4th ser., Water Resource Rept. 40.

Nickelsen, R. P. (1963), Fold patterns and continuous deformation mechanisms of central Pennsylvania folded Appalachians, in Tectonics and Cambro-Ordovician stratigraphy in the central Appalachians of Pennsylvania, Pittsburgh Geo!. Soc. and Appalachian Geo!. Soc., field conf. guidebook, Pittsburgh Pa., Pittsburgh Geo!. Soc., p. 13-29.

Peltier, L. C. (1949), Pleistocene terraces of the Susquehanna River, Pennsylvania, Pa. Geol. Survey, 4th ser., Gen. Geology Rept. 23.

Sevon, W. D. (1969), The Pocono Formation in northeastern Pennsylvania, Guidebook, 34th Annual Field Conf. Pa. Geologists. Pa. Geo!. Survey.

Sevon, W. D., Crowl, G. H., and Berg, T. M. (1975), The Late Wisconsinan drift border in northeastern Pennsylvania, Guidebook, 40th Annual Field Conf. Pa. Geologists, Pa. Geo!. Survey.

Sisler, J. D., Fraser, T., and Ashmead, D. C. (1928), Anthracite culm and silt, Pa. Geo!. Sur. vey, 4th ser., Mineral Resource Rept. 12.

GLOSSARY 33

Walker, R. G., and Harms, J. C. (1971), The "Catskill Delta, " a prograding muddy shoreline in central Pennsylvania, Jour. Geology, v. 79, p. 381-399.

White, I. C. (1883), Geology of the Susquehanna River region in the six counties of Wyoming, Lackawanna, Luzerne, Columbia, Montour, and Northumberland, Pa. Geo!. Survey. 2nd ser., Rept. G7.

Williams, E. H. (1895), Notes on the southern ice limit in eastern Pennsylvania, Am. Jour. Sci., 3rdser., v. 49, p. 174-185.

Wood, G. H., Jr., and Bergin, M. J. (1970), Structural controls of the anthracite region, Pennsylvania, in Fisher, G. W., and others, eds., Studies of Appalachian geology, central and southern, New York, Interscience, p. 147-160.

GLOSSARY

Clast. An individual grain or fragment of a sediment or rock. Decollement. A detachment surface upon which large-scale sliding has

taken place as a result of crustal deformation; strata above and below the detachment exhibit independent styles of deformation.

Efflorescent. Pertaining to minerals that change to powder from loss of water of crystallization.

Eolian. Pertaining to the wind and to sediments that are transported and deposited by the wind.

First-order fold, second-, third-, fourth-order folds. A classification of folds of different sizes by wavelength_ First-order-6 to 12 miles (10 to 20 km); second-order-0.6 to 6 miles (1 to 10 km); third-order-66 feet to 0.6 mile (20 m to 1 km); fourth-order-8 inches to 66 feet (20 em to 20m).

Glaciofluvial. Pertaining to meltwater streams flowing from glaciers or to the deposits made by such streams.

Glaciolacustrine. Pertaining to lakes that are marginal to glaciers and to the sediments deposited in such lakes.

Intertidal. Pertaining to the seashore area between mean high tide and mean low tide.

Orogeny. A period· of mountain building; also the process by which the structures (folds, faults, etc.) within mountain areas are formed.

Periglacial. Pertaining to the region or environment adjacent to a glacier. Pickeringite. Hydrated magnesium aluminum sulfate. MgAll

(SO.).·22H20; characterized by its astringent taste. Prograding shoreline. A shoreline that is being built outward into the sea by

deposition and accumulation of sediment. Slickenside. A polished and smoothly striated surface that results from fric

tion along a fault plane. Individual striations on this surface are called slickenlines (Fleuty, 1975).

Subtidal. Pertaining to shallow sea bottoms that lie between mean low tide and a depth of about 300 feet (90 m).

--


Supratidal. Pertaining to the seashore area just above mean high tide. Turbidite. A sediment or rock deposited from a bottom-flowing current

laden with suspended sediment; generally characterized by graded bedding and a distinctive vertical sequence of primary structures. Proximal turbidites are deposited near the source area of the sediment, whereas distal turbidites are deposited far out in the sedimentary basin.


Supratidal. Pertaining to the seashore area just above mean high tide. Turbidite. A sediment or rock deposited from a bottom-flowing current

laden with suspended sediment; generally characterized by graded bedding and a distinctive vertical sequence of primary structures. Proximal turbidites are deposited near the source area of the sediment, whereas distal turbidites are deposited far out in the sedimentary basin.

Documents

Geology and Mineral Resources of the Berwick Quadrangle, … · 2012-12-02 · 31 landscape. The major mineral resource in the Berwick area is sand and gravel. 'emendous quantities