United States
              Environmental Protection
              Agency
                Great Lakes
                National Program Office
                230 South Dearborn Street
                Chicago, Illinois 60604
EPA-905/9-91-005D-
GL-07D-91
oEPA
Genesee River
Watershed  Study
Volume IV — Special Studies
U.S.  Geological Survey
                                                  Printed on Recycled Pape

-------
              CENESEE  Rl VER  WATERSHED  STUDY
VOLUME 1:   Summary
VOLUME 2:  Special Studies -  New York\State
    REPORT I:  Sediment Nutrient  and
               Heavy M^tal Character! zati

    REPORT II:  Geo/Themi st ry of Oxide Pre
                Genfesee Watershed

    REPORT III:  Sdrficial Geology ofy^he Genesee Valley
 and Water Col umn
n in the Genesee River

i pi t at es in the
VOLUME 3:  Special Studies -  Renssel^er  Polytechnic Institute
           and Cornell Uni versi t

    REPORT I :   ITTvlentory of fiprms  of  Nutrients Stored in a
               Watershed

    REPORT II:  Evaluation of  thekEogardi  T-3 Bedl oad Sampler

    REPORT II i:  Nitro^n and  Phosphorus in Drainage Water
                 from OrgVni c  SoiRs
VOLUME 4:  Special Studies^-  United  States Geological  Survey

    PART I :   Streamflow and Sediment  Transport  in the Genesee
             Ri ver, New York

    PART II:  Hydrogeol ogi c Influences  on Sediment-transport
              Patterns in the  Genesee River Basin

    PART III:  Sources and Movement  of  Sediment in the
               Canaseraga Creek  Basin near Dansville,  New York

-------
                                                                   EPA-905/9-91-005D
                                                                   February 1 991
                     GENESEE RIVER WATERSHED STUDY
                            SPECIAL STUDIES
                    UNITED STATES GEOLOCIAL SURVEY
                               VOLUME 4
                                 for
            United States Environmental Protection Agency
                          Chicago, Illinois
                       Grant Number R005144-01

                           Grants Officer
                        Ralph G. Christensen
                 Great Lakes National Program Office
This study, funded by a Great Lakes Program grant from the U.S. EPA,
was conducted as part of the TASK C- Pilot Watershed Program for the
International Joint Commision's Reference Group on Pollution from
Land Use Activities.
                 GREAT LAKES NATIONAL PROGRAM OFFICE
              ENVIRONMENTAL PROTECTION AGENCY, REGION V
                      230 SOUTH DEARBORN STREET
                       CHICAGO, ILLINOIS  60604
                                            605 i^

-------
                  DISCLAIMER





This report has been reviewed by the Great Lakes National



Program Office, U.S. Environmental Protection Agency, and



approved for publication.  Approval does not signify that



the contents necessarily reflect the views and policies



of  the  U.S. Environmental  Protection Agency  nor does



mention of trade names or commercial products constitute



endorsement or recommendation for use.

-------
                      PART I

       STREAMFLOW AND SEDIMENT TRANSPORT IN THE
            GENESEE RIVER BASIN, NEW YORK


     Lawrence J. Mansue and William R. Bauersfeld
                U.S. Geological Survey
                   Ithaca, New York
           Prepared in cooperation with  the
New York State Department of Environmental Conservation
               Bureau of Water Research
                   Albany, New York

         U.S. Environmental Protection Agency
                 Chicago, Illinois

-------
                            CONTENTS - PART I
Abstract	   i
Figures	  ii
Tables	  iv
Conversion factors and abbreviat ions	   v
Acknowledgment s	  vi

      1.  Introduction	   1
             Objectives	   1
             Approach	   2
      2.  Conclusions...	   3
      3.  Physiography of the Genesee River basin	   4
             Genesee River	   4
             Major tributaries..	   5
      4.  Methods of data collection	   6
             Precipitation measurement.	,..	   6
             Streamf low measurement	   6
             Suspended sediment measurement	   6
      5 .  Results of analyses	   9
             Precipitation.	   9
             Streamf low	  10
             Sediment transport	  10
                Suspended sediment	  10
                Streambed material	  15
                Mineralogy of sediment material	  15
             Streamf low- and sediment-duration analyses	  23
             Suspended sediment yield	  23
      6.  Discussion of suspended sediment discharge	  26

References	  28

-------

-------
                                    ABSTRACT

     Streamflow and rates  of  sediment  transport in the Genesee River basin
were measured at  32 stations  between 1975 and 1977, and sediments were ana-
lyzed to determine their source  and role in the basin's sediment-transport
patterns.

     The stream-sediment loads and  composition were found to be related to
natural factors such as precipitation  and local geology.  Headwater areas,
where stream gradients are steepest and where easily eroded unconsolidated
glacial deposits  are extensive,  supply most of the sediment load.  Deposition
occurs in the lower half of the  Genesee River, where stream gradients are
flattest.

     Sediment loads transported  by  the Genesee River in New York during the
study were greatest at Portageville and Mount Morris, about midway down the
river, and at Rochester, near the river mouth at Lake Ontario.  The greatest
annual sediment loads at those sites ranged from 1 to 1.4 million megagrams.
The largest annual sediment yields  measured during the study were at
Portageville, Mount Morris, and  Avon,  where these yields ranged from 200 to
400 megagrams per square kilometer.

     The sediments transported by streams in the Genesee basin were mostly
silt-sized particles composed largely  of quartz (16-86 percent); clay minerals
in the finer sediment load were  mostly llllte (10-55 percent) and chlorite
(6-16 percent).   Percentage ranges  were greater In streambed-transported
materials than in suspended sediments.
                                     I-i

-------
                                    FIGURES

                             (at back  of  report)

Number                                                                    Page

   1      Map of Genesee River basin showing  locations of data-
         collection  sites	   29

   2      Long-term average monthly precipitation for period of
         record (1941-70)  and  monthly precipitation  from January
         1975-September 1977 at Wellsville,Dansville and Rochester	    30

   3      Instantaneous streamflow and suspended sediment curves
         for  27 stations  in the Genesee River basin:
             A.  Genesee  River  at  Wellsville......	  31
             B.  Genesee  River  at  Transit Bridge near Angelica....	  31
             C.  Genesee  River  near Houghton	  32
             D.  Genesee  River  at  Portageville	  32
             E.  Sugar  Creek  near  Canaseraga	  33
             F.  Canaseraga Creek  above Dansville	  33
             G.  Stony  Brook  at Stony Brook State Park....	  34
             H.  Mill Creek at  Patchinville	  34
             I.  Mill Creek at  Perkinsville	  35
             J.  Mill Creek near Dansville	  35
             K.  Mill Creek at  Dansville	  36
             L.  Canaseraga Creek  at Groveland	  36
             M.  Bradner  Creek  near Dansville	  37
             N.  Bradner  Creek  near Sonyea	  37
             0.  Keshequa Creek at Nunda	  38
             P.  Keshequa Creek at Tuscarora	  38
             Q.  Keshequa Creek at Sonyea	  39
             R.  Canaseraga Creek  at Shakers Crossing	  39
             S.  Genesee  River  near Mount Morris	  40
             T.  Genesee  River  at  Avon	  40
             U.  Oatka  Creek  at Rock Glen	  41
             V.  Oatka  Creek  at Warsaw	  41
             W.  Pearl  Creek  at Pearl Creek....	  42
             X.  Oatka  Creek  near  Pavillion Center	  42
             Y.  Mad Creek near Le Roy	  43
             Z.  Oatka  Creek  at Garbutt	  43
             AA.  Genesee  River  at  Rochester	  44
                                     I-ii

-------
                             FIGURES  (continued)
Number                                                                    Page

   4     Duration curves showing long-term mean  daily  streamflow
         and June 1975 to May 1977 mean daily  streamflow,  suspended
         sediment concentration, and suspended sediment  discharge at
         Genesee River basin stations:

             A.  Genesee River at Wellsville	   45
             B.  Genesee River at Portageville.	   46
             C.  Canaseraga Creek above Dansvilie  (streamflow only)	   47
             D.  Keshequa Creek at Sonyea (streamflow  only)	   48
             E.  Canaseraga Creek at Shakers Crossing	   49
             F.  Genesee River near Mount Morris.	   50
             G.  Genesee River at Avon	   51
             H.  Oatka Creek at Warsaw (streamflow only)	   52
             I.  Oatka Creek at Garbutt	   53
             J.  Genesee River at Rochester....	   54
                                    I-iii

-------
                                  TABLES
Number
         Stations at which streamflow and suspended sediment were
         measured in the Genesee River basin in water years  1975-
         1977	    7

         Monthly suspended sediment discharge in the Genesee River
         and selected tributaries, 1975-1977.,	  11

         Average slope of sediment-transport curve, at discharge of
         0.10 cubic meters per second per square kilometer,  for 27
         stations in the Genesee River basin, 1975-1977(curves ate
         shown in Fig. 3)	  13

         Particle size distribution of suspended sediments at
         selected sampling stations, Genesee River basin, 1975-77....  14

         Mineralogical analyses of sediment material, Genesee River
         basin, 1975-1977	  16

         Calculated average annual suspended sediment load,
         Genesee River at Rochester, based on 1953-77 streamflow
         and 1975-77 sediment water year records	  24

         Drainage area and average annual suspended sediment load
         and yield at stations sampled in Genesee River basin	  25
                                     I-iv

-------
           FACTORS FOR CONVERTING  INTERNATIONAL  SYSTEM (SI)  UNITS
               TO INCH-POUND UNITS  AND ABBREVIATIONS  OF UNITS
Multiply SI unit

kilometer  (km)

meter (m)



square kilometer  (km2)
cubic hectometer
megagram  (Mg)
cubic meter  per  second
  (m3/s)
meters  per  kilometer  (m/km)



megagram/km2
cubic meters  per  second  per
  square  kilometer  [(m^
   to

  0.6214

  3.281

  Area

  0.3861

 Volume

810.7

  Mass

  1.102

  0.9842

  Flow

 35.31
                    to obtain inch-pound unit

                    mile (mi)

                    foot (ft)



                    square mile (mi2)



                    acre-foot (acre-ft)



                    ton [short, 2,000 pounds (lb)]

                    ton [long, 2,240 lb]
                    cubic foot per second
                      (ft3/s)
              feet per mile  (ft/mi)
        Slope

        5.28

Specific Combinations

        2.85        ton (short)/mi2

        2.55        ton (long)/mi2
  91.45
                    cubic feet per  second  per
                       square mile  [(ft3/s)/mi2]
                                     I-v

-------
                                ACKNOWLEDGMENTS

     This study was carried  out as  part  of Task C of the Pollution from
Land Use Activities Reference Group,  International Joint Commission and was
funded through the U.S. Environmental Protection Agency and the State of
New York.

     The authors acknowledge the  guidance, support, and advice received from
Drs. Leo J. Hetling and G. Anders Carlson of the New York State Department
of Environmental Conservation, and  Robert B. Dona, Project Officer of the
U.S. Environmental Protection Agency.  The authors are also grateful to the
Buffalo District, U.S. Army  Corps of  Engineers, for providing financial
support, under another program, for the  daily-streamflow stations that
supplied data in this report.  The  authors acknowledge the advice and coop-
eration by George Pericht, of the National Weather Service, who provided
weather data during this  study.

     Sediment observations were made  by local residents Ralph Bishop, Frank
Blue, Arlene Buckley, Arnold Downey,  Rodney Graham, Frank Keller, Charles
Nadeau, E. William Prytherch, Philip  Swartout, and Gloria Williams.  Their
assistance is greatly appreciated by  the authors.
                                      I-vi

-------
                                    SECTION I

                                  INTRODUCTION

     Concern over  the deterioration of water quality of the Great Lakes led
the Governments of  the United  States and Canada to conduct studies of the
effects of land use  on the  water  quality of the Great Lakes.  The Great Lakes
Water Quality Agreement  of  April  15, 1972, empowered the International Joint
Commission (IJC) to  authorize  such studies and the development of recommenda-
tions for remedial measures.   Through the Great Lakes Water Quality Board, the
IJC established the  International Reference Group on Great Lakes Pollution
from Land Use Activities (Pollution from Land Use Activities Reference Group-
PLUARG) to carry out such studies.

     PLUARG developed a  program consisting of four major tasks:  Task A, to col-
lect and assess management  and research information and, in its later stages,
to critically analyze the potential implications of recommendations; Task B,
to prepare a land-use inventory and an analysis of trends in land-use patterns
and practices; Task  C, to carry out (1) detailed surveys of selected water-
sheds to determine  pollutant  sources and their relative significance, and (2)
to assess the transport  of  pollutants to boundary waters; and Task D, to ob-
tain supplementary  information on the effects of suspended materials on the
boundary waters, their effect  on  water quality, and their future significance
under alternative  management  schemes.  The PLUARG study plan was approved by
the Great Lakes Water Quality  Board in March 1974 and by the IJC in April 1974.

     Task C included intense  investigations of six watersheds in Canada and
the United States  that represent  the full range of urban and rural land uses
in the Great Lakes  basin.  A technical committee and a Task C subgroup deve-
loped and conducted  pilot watershed studies and studies of the rates and pat-
terns of the transport of selected pollutants to Lake Ontario, particularly
suspended sediment,  phosphorus, and chlorides.  The Genesee River basin was
selected for study by the U.S. Geological Survey to quantify the effects of
(a) land-use activities, (b)  soils, and (c) geology and geomorphology, on
surface-water quality.

OBJECTIVES

     The U.S. Geological Survey's program in the Genesee River basin con-
sisted of (a) establishment of a  data-collection network, and (b) the collec-
tion, analysis, and  interpretation of streamflow and sediment data, including
a study of sediment-source  material and patterns of deposition.  In this
report, only daily and partial-record streamflow data, suspended-sediment data,
and mineralogical  data collected  from the Genesee River and its major tribu-
taries are tabulated; interpretations of these data are given in Part II of
this volume (Mansue, Young and Soren, 1983).

                                      1-1

-------
APPROACH

     Seven daily,  24 partial,  and  2  miscellaneous suspended-sediment records
were compiled from samples  collected at  sites  in the Genesee River basin
between 1975 and 1977.  Recording  precipitation gages provided instantaneous
information from the headwaters  of two major tributary streams near Arkport
and Warsaw by automatic telephone  transmission.  Mineralogical analyses of
sediment "samples were done  to  determine  the spatial and seasonal variations
in mineral content of suspended  sediment in the river.
                                     1-2

-------
                                    SECTION 2

                                   CONCLUSIONS

     The greatest measured  suspended-sediment discharge in the Genesee River
basin from April 1975  to  September 1977 was in the Genesee River at
Portageville.  The highest  monthly sediment loads occurred in February 1976 at
Wellsville (22,000 Mg)  and  at  Portageville (666,000 Mg), during which time 62
percent of the total sediment  load for the 1976 water year was transported.
The highest measured monthly  suspended-sediment yield (load per drainage area)
was in the Genesee River  at Portageville in February 1976 (262 Mg/km2) and in
Canaseraga Creek at Shakers Crossing in September 1977 (109 Mg/km2).

     In general, the greatest  suspended-sediment discharge per unit of stream-
flow occurred in the upper  reaches of streams; deposition occurred at sites
further downstream.  Data collected from the Genesee ma instern suggest a lag in
sediment transport in  the river system.  On a daily-measurement basis, a lag
in the migration of the suspended sediment after storms was noted, which indi-
cates a month or more  of  lag  in the downstream movement of sediment in the
lower part of the basin.

     The major mineral  constituents transported by streams within the basin
are quartz, illite, and chlorite.  No seasonal variation was detected in the
mineralogical content  of  the  sediments.
                                      1-3

-------
                                    SECTION 3

                      PHYSIOGRAPHY OF GENESEE RIVER BASIN

     The Genesee River  originates in Potter County, Pa., near the New York
boundary, and  flows  north  through western New York into Lake Ontario, draining
an area of 6,394 km^.   The river basin includes part of Potter County,  Pa.,
most of Allegany and Livingston Counties, N.Y., and parts of Wyoming, Ontario,
Monroe, and Genesee  Counties,  N.Y.   A map of the basin showing the  location
of data-collection  sites  is given in figure 1.

     Sedimentary rocks  of  Ordovician, Silurian, and Devonian ages (from north
to south) underlie  the  Genesee River basin.  The rocks strike east-west and
dip southward  at low angles.   Shale, siltstone, and limestone predominate  in
the northern part;  siltstone and sandstone predominate in the southern  part.

     In the northern (lower) part of the basin, the rocks are less  resistant
to erosion than in  the  southern part; also, the terrain is relatively even, and
stream gradients are low.   In the southern (upper) part of the basin, more  resist
ant rocks form highlands  of greater relief than in the lower part,  and  stream
gradients in the upper  basin are steeper.  Stream gradients lessen  markedly
northward from about the  vicinity of Mount Morris.

GENESEE RIVER

     The Genesee River  begins at an altitude of about  610 m and  flows 235  km
northward, entering  Lake  Ontario at an altitude of about 74 m.   Many tributary
streams contribute  to the  Genesee's flow.  The largest of the tributaries  are
Canaseraga and Oatka Creeks (fig. 1).

     Flow of the main stem is unregulated from the river's origin to the dam
at Mount Morris Lake (U.S. Army Corps of Engineers Flood Control Reservoir)
near Mount Morris.   This  reservoir has a maximum length of 24 km, with  a
usable storage capacity of 415 hm^ and a dead storage  of 0.751 hm^.  A  dam for
generating hydroelectric  power is downstream at Mount  Morris.  At Rochester,
the river is affected during the navigation season by  the Erie (Barge)  Canal,
at the southern end  of  the City, where the barge-canal pool is regulated by a
gated  dam operated  by New York State.  Further downstream, the river has three
controlled ponds and diversions for electric-power generation in the City of
Rochester.
                                      1-4


-------
     Several of  the Genesee  River's tributary streams are regulated by
dams for water supply  or  recreation,  or both.  The major impoundments are
on Caneadea Creek near Caneadea (Rushford Dam), WLscoy Creek near Wiscoy,
in the west-central part  of  the Genesee basin, and at Conesus, Hemlock,
Canadice, and Honeoye  Lakes  on tributaries in the east-central part of
the basin. .
MAJOR TRIBUTARIES

Canaseraga Creek

     Canaseraga Creek  originates in the east-central part of the basin  in
Steuben County (fig. 1)  and flows generally northwest to the Genesee River
near Shakers  Crossing.   Canaseraga Creek is 68 km long and drains an area
of 868 km^.   The Canaseraga Creek subbasin includes several tributaries,
the largest of which are Mill and Keshequa Creeks.

Oatka Creek

     Oatka Creek originates in Wyoming County, in the west-central  part
of the Genesee basin  (fig.  1), and flows northwest to the Genesee River.
Oatka Creek is 96 km long and drains an area of 557 km^.  It is partially
regulated by  a dam  at  Le Roy.
                                     1-5

-------
                                   SECTION  4

                          METHODS OF  DATA COLLECTION

     Precipitation, streamflow,  and sediment data for this report were
collected at 32 sites on  the Genesee  River  and its major tributaries from
November 1974 to September  1977.  Pertinent earlier data were also included.
The locations of the data-collection  sites  are shown in figure 1; measurements
made at the stations and  periods during which data were collected are given in
table 1.

PRECIPITATION MEASUREMENT

     Recording precipitation gages were installed near Arkport and Warsaw, at
the two principal  tributary headwater sites, to obtain telemark (instantaneous
telephone translation)  rainfall  values.  (Arkport is outside the Genesee basin
(fig. 1); however,  the  "Arkport" gage is actually in the basin, about 1 1/2 km
west of South Dansville.)  This  information was needed to correlate streamflow
and sediment measurements with  runoff from  headwater drainage and also pro-
vided information  on precipitation quantity and Intensity during the data-
collection period.

STREAMFLOW MEASUREMENT

     Streamflow was measured monthly  and during high-flow periods at all sites
to define the relationship  of  stream  stage  to discharge.  At each daily
streamflow-record  station,  a graphic  or digital recorder provided a continuous
record of the gage height (water-surface elevation).  Values of mean daily
streamflow were computed  from  rating  curves that establish a relationship bet-
ween stream stage  and  discharge.

     Partial-record streamflow stations consisted of a reference gage to
measure gage height, and  a  crest-stage gage to record the maximum stream
stage.  Instantaneous  streamflow at  partial-record sites either was measured
or was computed from stage-to-discharge relationships.

SUSPENDED-SEDIMENT MEASUREMENT

     Suspended-sediment samples  were  analyzed at the U.S. Geological Survey
sediment  laboratory in Ithaca,  N.Y.,  by methods outlined in Guy  (1969).
Record computations were  made  in accordance with techniques described by
Porterfield (1972).
                                      1-6

-------
TABLE 1.  STATIONS AT WHICH STREAMFLOW AND SUSPENDED SEDIMENT WERE MEASURED IN THE
                     GEKESEE RIVER BASIN, HATER YEARS 1975-77




04221000

04221725

04222300
04223000
04224740
04224775
04224848
04224900
04224930
04224940
04224978
04225000

04225500

04225600
04225670
04225915
04225950
04226000

04227000

04227500
04228370
04228380
04228500
04230320
04230380
04230400
04230410
04230423
04230470
04230SOO
04231000
04232000

«
Station number and name*
Genesee River at Wellsville

Gene see River at Transit Bridge
near Angelica
Genesee River near Boughton
Genesee River at Portageville
Sugar Creek near Canaseraga
Canaseraga Creek above Dansville
Stony Brook at Stony Brook State Park
Mill Creek at Patchinvllle
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Canaseraga Creek near Dansville

Canaseraga Creek at Groveland

Bradner Creek near Dansville
Bradner Creek near Sonyea
Keshequa Creek at Nunda
Keshequa Creek at Tuscarora
Keshequa Creek at Sonyea

Canaseraga Creek at Shakers Crossing

Genesee River near Mount Morris
Little Conesus Creek near South Lima
Little Conesus Creek near East Avon
Genesee River at Avon
Oatka Creek at Rock Glen
Oatka Creek at Warsaw
Oatka Creek at Pearl Creek
Pearl Creek at Pearl Creek
Oatka Creek near Pavlllion Center
Mad Creek near Le Roy
Oatka Creek at Garbut
Black Creek at Churchville
Genesee River at Rochester
Streamflow
(daily
record)
8/55-9/58,
10/72-9/77
—

—
8/08-9/77
—
8/74-9/77
—
—
—
—
—
7/10-9/35,
7/70-9/76
2/17-3/20,
10/55-9/64
—
—
_
—
3/11-9/32,
11/74-9/77
11/59-9/70,
10/74-9/77
6/03-9/77
—
—
8/55-9/77
—
12/63-9/77
—
—
—
—
10/45-9/77
10/45-9/77
12/19-9/77
Sediment
(daily
record)
4/75-9/77

—

—
4/75-9/77
—
—
—
—
—
—
—
—

_
—
—
—
—
--.
—

3/75-9/77

4/75-9/77
—
—
4/75-9/77
—
—
__
—
—
—
3/75-9/77
—
4/75-9/77
Streamflow
(partial
record )
«

2/75-9/77

4/77-9/77
—
2/75-9/77
—
12/74-9/77
7/76-9/77
7/76-9/77
7/76-9/77
12/74-9/77
—

12/74-9/77
12/74-9/77
12/74-9/77
12-74-9/77
12/74-9/77
12/74-9/77
—

—

—
2/75-6/76
2/75-6/76
—
12/74-9/77
—
12/74-9/76
12/74-9/77
12/74-9/77
12/74-9/77
—
—
—
Sediment
(partial
record)
__

2/75-9/77

4/77-9/77
—
2/75-9/77
12/74-9/77
12/74-9/77
7/76-9/77
7/76-9/77
7/76-9/77
12/74-9/77
12/74-9/76

12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77

—

—
2/75-6/76
2/75-6/76
—
12/74-9/77
12/74-9/77
12/74-9/76
12/74-9/77
12/74-9/77
12/74-9/77
—
12/74-6/76
—

note: Refer to text for definition of station
type.



* Locations are shown in figure 1>
                                       1-7

-------
     At daily suspended-sediment  record  stations,  a depth-integrating sampler
was suspended by a  cable  from a reel  at  a fixed  location.   Stream cross-
section samples were  obtained monthly and during high flows to verify values
of the single vertical  sample at  the  fixed location.   Single vertical samples
were collected  (a)  daily  when flows were uniform,  (b) at about 2-hour inter-
vals when flows were  increasing rapidly  during storms, and (c) at 4- to 6-hour
intervals during the  streamflow recession.  The  sampling devices used were of
designs by the  (U.S.J Water Resources Council (1975).  Mean daily-sediment
concentration and streamflow values were used to determine dally sediment
loads except for periods  of rapidly changing flow, for which a method of sub-
division was used to  compute daily sediment loads (Porterfield, 1972, p. 47-52).

     Samples at partial-record stations  were collected during periods of storm
runoff and monthly  during low flows to provide Instantaneous suspended-
sediment Information.   Instantaneous  sediment discharges were computed from a
stage-to-discharge  relationship of measurements  or, when data were incomplete,
were estimated  from other stage-to-discharge measurements.

     Samples at miscellaneous suspended-sediment stations were collected by
New York State  personnel  monthly  and  when water  samples were obtained for
chemical and metals analyses.
                                      1-8

-------
                                    SECTION 5

                               RESULTS OF ANALYSES

PRECIPITATION

     The  precipitation data collected from the two telemark stations near
South Dansville  ("Arkport"  station) and Warsaw during the study provided
supplemental data.   Records from three National Weather Service stations
(Wellsville, Dansville,  and Rochester) were used to determine the long-term
(1941-70)  precipitation patterns in the Genesee River basin.  Graphs showing
monthly totals  for  the long-term record and for 1975-77 are presented in
figure 2.

     Precipitation  at  the three National Weather Service stations is generally
lowest in  February  and greatest in July.  The precipitation patterns from 1975
to 1977 were as  follows:

     1975.—Monthly precipitation at Wellsville, Dansville, and Rochester
ranged from less than  the long-term average to the long-term average in
January, March,  April,  July,  September, October, and November.  In May,
monthly precipitation  at  Dansville and Rochester was of long-term average
intensity; however,  precipitation was significantly greater than the long-term
average at Wellsville.   At  all three stations, precipitation was significantly
greater than the long-term  average during February, June, August, and
December.

     1976.—Total monthly precipitation was equal to or above the long-term
average in January,  February,  March, June, July, August, and October.
Precipitation in April exceeded the long-term averages at Dansville and
Rochester  but was lower at  Wellsville.  The total precipitation at the three
stations during  May and September ranged from about the same as to slightly
less than  the long-term averages; however, the precipitation in November and
December were substantially less than the long-term averages.

     1977.—Total precipitation in the first half of 1977 was less than the
long-term average at Dansville and Rochester but was about average at
Wellsville.  In  June,  precipitation was greater than the long-term average at
all stations.  Total precipitation in July, August, and September was signifi-
cantly greater than the  long-term average except at Rochester, where precipi-
tation in  July was  less  than  the long-term average.
                                      1-9

-------
STREAMFLOW

     Mean daily, monthly,  and  annual  streamflow values were calculated from
data collected at continuous gaging stations.   The mean daily values were used
to describe the  streamflow variation  in time with duration analyses.
(Analyses of the long-term record and the 1975-77 period are given in graphs
in figure 4.)

     Instantaneous  streamflow  values  at all stations were measured or com-
puted to provide discharge data  as an independent variable for use in com-
puting sediment  discharge. The  streamflow values were used in association
with data on sediment-transport  rates.  Graphs showing the relation of
streamflow to suspended-sediment discharge at the various measurement sites
are presented in figure  3.
SEDIMENT TRANSPORT

     Sediment  in  a  stream is  carried by suspension, saltation, and bedload
transport,  or  a combination of these processes.  Suspended sediment is carried
in the  stream  above its  bed;  saltation moves particles in a series of hops
along the  stream  bottom,  and  bedload transport is the movement of particles
along the  stream  bottom  by rolling or sliding.

Suspended  Sediment

     Monthly suspended-sediment loads, derived from the daily records, are
given in table 2.   Suspended-sediment yield (load per unit area) generally
decreases  downstream in  the Genesee River basin.  From April to September
1975, the  yield at  Portageville was about 7.5 times greater than at Rochester.
During  the equivalent period  in 1976, the yield was about 1.5 times greater  at
Portageville than at Rochester, and, from April to September 1977, the yield
at Portageville was about 2.5 times greater than at Rochester.  The total
annual  suspended-sediment discharge at each of these sites during 1976 was
about the  same as in 1977, but the total annual yield at Portageville was
about 2.5  times greater  than  at Rochester.  The greatest annual suspended—
sediment discharges by the Genesee River during the study were at
Portageville,  Mount Morris, and Rochester, and ranged from 1 to 1.4 Mg.  The
largest annual sediment  yields in the river during the study occurred at
Portageville,  Mount Morris, and Avon, and ranged from about 200 to 400 Mg/km^.

     Decreasing sediment yield as drainage area increases in the downstream
direction  is a phenomenon that has been observed in many streams (Walling,
1976, p. 19).  This pattern reflects the geomorphologic processes of erosion
(degradation)  in  the headwaters, where river gradients are steeper, and  aggra-
dation  downstream,  where river gradients are lower.
                                      1-10

-------
            TABLE 2.  MONTHLY SUSPENDED-SEDIMENT LOAD IN THE GENESEE RIVER AMD SELECTED TRIBUTARIES, 1975-77
                                                    (In rnegagroms).


	Monthly totals	      1975-77
Year     OCT.   HOV.     PEC.    JAN.    FEB.     MAR.    APR.     MAY      JPNE     JULY    AUG.    SEPrT      YEARLY"

STATION 04221000i',, GENESEE RIVER AT WELLSVILLE (Drainage area 749 km2)

1975      __     __       __      —      —       —       214    1,130   12,200     102     249    13,600

1976     1,500    259   1,400     121   22,000    5,890     454    1,760    1,100     389     619       157      35,600

1977     5,960    724     238      46    2,090    6,910     862    1,360      785  10,900   1,860    20,700      52,500


STATION 04223000, GENESEE RIVER AT PORTAGEVILLE (Drainage area 2,541 km2)

1.975      _     _       _      _               —     7,120  288,000  252,000     426   2,010   116,000

1976    34,400  1,450  73.300  33,300  666,000  176.000  35,600    5,420   14,100  18,200  17,200       797   1,080,000

1977    80,800  5,650   1,080     382   37,100  183,000 126,000   12,800      866 118,000  85,000   441,000   1,090,000


STATION 04227000, CANASERAGA CREEK AT SHAKERS CROSSING (Drainage area 862 km2)

1975      __     __       _____       __       989   38,000   12,900     149     805     9,620

1976     6,620    351   8,540   4.730   82,600   76,600  22,700    1,790    1,260   2.350   7.670       183     215,000

1977    18,600  1,620     387      41    9,380   24,400  41,400    5,630      631  21,300  12,000    94,000     229,000


STATION 04227500, GENESEE RIVER NEAR NT. MORRIS (Drainage area 3,670 km2)

1975      —              _____       _    23,700  121,000  110,000     793   3,650   125,000

1976    60,500  3,760  48,900   8.860  138.000  306,000  68,200   20,200   18,100  26,800  21,000     1,020     721,000

1977   113,000 39,400  12,900   2,800   18,300  282,000 145,000   42,000    2,940 112,000 132,000   346,000   1,260,000


STATION 04228500, GENESEE RIVER AT AVON (Drainage area 4,318 tan2)

1975      —     —       —      —      --       —    33,100  102,000  114,000   1,650   1,550    90,700

1976    33,300  2,850  45.800   6,880  214,000  174,000  84,000   32,300   15,400  26,900  27,600       998     664,000

1977    68,900 32,900   3,400     409    5,840  189,000 133,000   33,500    2,260 106,000  97,500   251,000     924,000


STATION 04230500, OATKA CREEK AT GARBUTT (Drainage area 528 km2)

1975      —              —      —               —       129      189      593      17      24        11

1976        26     29     758     249    4,830    5,000     868      262      204     152     286        25      12,700

1977       124    216      71      40       89    2,380   1.080      104       39     376   1.610     2,980       9,100


STATION 04232000, GENESEE RIVER AT ROCHESTER (Drainage area 6,364 km2)

1975      —     —       —      —      —       —    15,700   64,000   77,800   2,190   2,530    53,900

1976    26,000  3,870  54,400   5.650  468.000  353,000  76,800   19,800    7,470  11,400  27,700     1.560   1,060,000

1977    53,400 20,200   2.640   1,260    6,570  247,000 129,000    7,950    1,310  65,400  76,500   437,000   1,050,000


II  Station  locations are shown  in  figure 1.
                                                         I'll

-------
     Large areas of easily  eroded,  unconsolidated deposits upstream from
Portageville are a major  source  of  sediment  in the Genesee River.  The river
gradient is steepest  from Portageville  to the  Pennsylvania border, where it
averages about 2.2 m/km.  Material  eroded from these areas is deposited both
above the Mount Morris  dam  and further  downstream, where the river gradients
are lower.  Downstream  from Portageville, between Geneseo and Avon, the chan-
nel gradient is about 0.2 m/km.   Further downstream, between Avon and
Rochester, the river  gradient decreases to about 0.02 m/km.

Relationship of Suspended-Sediment  Transport to Streamflow.—The relationship
between streamflow and  suspended sediment is described by Colby (1956).
Suspended-sediment-transport  curves,  plotted from data obtained at 27 stations,
are shown in figure 3.  The slopes  of the curves represent suspended-sediment
discharge in relation to  stream  discharge.  The steeper the slope of the
curve, the greater the  proportion of  sediment  in transport.  For the purpose
of comparing the amount of  sediment in transport at the different stations in
figure 3, a point of  tangency on the  curves at which streamflow equals 0.10
[(m3/s)/km2] was used to  normalize  the slopes.  The average slopes are given
in table 3.

     Four stations within the basin have curve slopes of 3 or greater, which
Indicates a relatively  high sediment  yield.   These stations and their curve
slopes are:

     Mill Creek at Patchinville, 5.9    Genesee River near Mount Morris, 5.5
     Mill Creek near  Dansvilie,  3.5    Genesee River at Avon, 3.9

Particle-Size Distribution.—Many of  the suspended-sediment samples collected
during the high flows were  analyzed for particle size; the extent of the ana-
lysis was determined  by the amount of sample material available.  At stations
with  low loads, it was  difficult to obtain sufficient material to represent a
sample.  At other  sites,  such as Portageville, which often had high con-
centrations, many  samples were  collected for particle-size determinations.
[Particle-size determinations were done in accordance with procedures
described in Guy  (1969, p.  28-45).J

     Arithmetic average values  of the particle-size analysis of  suspended-
sediment samples  collected  are  given in table 4.  The percentages are by dry
weight.  These averages assume  a linear distribution.  No  statistical analysis
was made to determine the representativeness  of  the size  fraction at each  sta-
tion.

      The percentage  of sand transported in suspension by  a stream is generally
in direct proportion to stream gradient and depends on the composition  proper-
ties  of  source material.   At Wellsville,  the  Genesee River transported  about
twice as much  sand as at  Portageville; this is probably because  the land being
eroded in  the  drainage area upstream from Wellsville consists  predominantly  of
sandy glacial  deposits and because the channel had  been disturbed by recent
construction  work in the  Wellsville vicinity.  In contrast,  considerable
amounts  of  glacial-lake sediments, predominantly of silt,  provide  the major
sediment  source  upstream from Portageville.
                                     1-12

-------
     The percentage  of  silt  transported in suspension past Portagevtlle
decreases downstream below the  Mount Morris dam, but the sand proportion
increases below  the  steep gradient of an ancient glacial lake delta further
downstream  (the  Genesee River flowed into the Canaseraga Valley basin, which
contained a glacial  lake).   The silt fraction retained in the reservoir at
Mount Morris and the amount  deposited below the delta have not been deter-
mined.  The determination is complicated because Canaseraga Creek, which
enters the  Genesee River below the delta but upstream from the Mount Morris
station, is a  source of much clay- and silt-sized material.

     The percentage  of  sand-sized material transported in suspension near the
Mount Morris station is reduced by one-half at Avon, which suggests con-
siderable sand deposition within this reach.  For much of the distance between
Geneseo and Avon, the stream flows on till with only a thin cover of alluvium
or glacial-lake  clays.

     TABLE  3.  AVERAGE  SLOPE OF SEDIMENT-TRANSPORT CORVES, AT DISCHARGE OF
               0.1 CUBIC METERS PER SECOND PER SQUARE KILOMETER, FOR 27
               STATIONS IN GENESEE RIVER BASIN, 1975-77
                            (Curves are shown in figure 3)


04221000
04221725
04222300
04223000
04224740
04224775
04224848
04224900
04224930
04224940
04224978
04225500
04225600
04225670
04225915
04225950
04226000
04227000
04227500
04228500
04230320
04230380
04230410
04230423
04230470
04230500
04232000
Station number and name
Genesee River at Wellsville
Genesee River at Transit Bridge near Angelica
Genesee River near Houghton
Genesee River at Portageville
Sugar Creek near Canaseraga
Canaseraga Creek above Dansville
Stony Brook at Stony Brook State Park
Mill Creek at Patchinville
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Canaseraga Creek at Groveland
Bradner Creek near Dansville
Bradner Creek near Sonyea
Keshequa Creek at Nunda
Keshequa Creek at Tuscarora
Keshequa Creek at Sonyea
Canaseraga Creek at Shakers Crossing
Genesee River near Mount Morris
Genesee River at Avon
Oatka Creek at Rock Glen
Oatka Creek at Warsaw
Pearl Creek at Pearl Creek
Oatka Creek near Pavillion Center
Mad Creek near Le Roy
Oatka Creek at Garbutt
Genesee River at Rochester
Average slope
1.9
2.7
2.7
2.6
2.9
2.3
2.7
5.9
2.9
3.5
2.4
2.5
1.9
1.8
2.1
2.4
2.5
2.3
5.5
3.9
2.7
2.7
2.4
1.6
1.9
1.9
2.8
                                     1-13

-------
TABLE 4.  PARTICLE-SIZE DISTRIBUTION OF  SUSPENDED  SEDIMENTS AT SELECTED
          SAMPLING STATIONS, GENESEE RIVER  BASIN,  1975-77

Average percentage
within sediment samples
Clay
Station number and name (<0.004
04221000 Genesee River at Wellsville
04221725 Genesee River at Transit Bridge
near Angelica
04222300 Genesee River near Houghton
04223000 Genesee River at Portageville
04224740 Sugar Creek near Canaseraga
04224775 Canaseraga Creek above Dansvllle
04224848 Stony Brook at Stony Brook State Park
04224900 Mill Creek at Patchinville
04224930 Mill Creek at Perkinsville
04224940 Mill Creek near Dansville
04224978 Mill Creek at Dansville
04225000 Canaseraga Creek near Dansville
04225500 Canaseraga Creek at Groveland
04225600 Bradner Creek near Dansville
04225670 Bradner Creek near Sonyea
04225915 Keshequa Creek at Nunda
04225950 Keshequa Creek at Tuscarora
04226000 Keshequa Creek at Sonyea
04227000 Canaseraga Creek at Shakers Crossing
04227500 Genesee River near Mount Morris
04228370 Little Conesus Creek near South Lima
04228380 Little Conesus Creek near East Avon
04228500 Genesee River at Avon
04230320 Oatka Creek at Rock Glen
04230380 Oatka Creek at Warsaw
04230410 Pearl Creek at Pearl Creek
04230410 Pearl Creek at Pearl Creek
04230423 Oatka Creek near Pavilllon Center
04230470 Mad Creek near Le Roy
04230500 Oatka Creek at Garbutt
04231000 Black Creek at Churchville
04232000 Genesee River at Rochester
26
27

37
32
32
26
27
22
—
22
17
27
22
48
43
38
36
31
44
38
--
--
40
—
28
—
—
—
—
61
—
35
Silt Sand
(0.004- (0.062-
mm) 0.062 mm) 2.0 mm)
50
55

54
54
51
62
59
65
—
46
60
47
56
44
55
51
51
55
43
46
—
—
48
—
50
—
—
—
—
28
— —
49
25
18

9
14
17
12
14
13
13
32
23
26
22
8
2
11
13
14
13
16
—
—
12
24
22
9
18
8
16
11
26
16
                                  1-14

-------
     Mill Creek at Perkinsvilie shows a low percentage of  sand  owing  to  the
 low gradients  upstream from this sampling site.  The small  amount  of  sand-
 sized  material transported by Bradner Creek near Dansvilie  is unexplained
 because  the  basin upstream from this site contains large amounts of  sand and
 gravel overlying dense gray till*  However, it is probable  that  the  very low
 gradient  of  Bradner Creek, a yazoo-type tributary to Canaseraga  Creek,  is  not
 capable  of'transporting significant quantities of sand, so  that  sand  brought
 down from the  upper part of Bradner Creek's basin is deposited  in  delta-like
 fashion  on entering the valley*  Oatka Creek shows a downstream  decrease in
 the amount of  sand loading; the low amount measured at the  Garbutt station is
 attributed to  the low gradients upstream and low-intensity  precipitation
 within the drainage area.

 Streambed Material

     Bed  material was collected from 16 stream sites for size and  mineralogi-
 cal analyses.   At sites on small streams, Streambed samples were collected
 directly  into  sample containers; at sites on larger streams, grab  samples  were
 obtained  from  several spot locations to provide a representative sampling  for
 the site.   Size and mineraloglcal analyses were also done on Streambed  samples
 from four separate stream reaches to define the spatial variation  and material
 gradation.   Collection was made by a nodal-point method (Wolman, 195A).
 Selected  samples containing an appreciable amount of fine sediment were  ana-
 lyzed  for mineral content to determine the sources.

 Mineralogy of  Sediment Material

     Samples of suspended sediment and bed and source material were obtained
 for mineral  analyses.   The suspended-sediment samples were  collected  over  a
 wide range of  runoff conditions; the bed material was collected  after a  sea-
 sonal  high-flow period.  Table 5 gives results of 274 mineralogical analyses
 from stream  sites,  in downstream order, followed by source  materials.

     The  results of the analyses are consistent with the type and  age of the
 rocks  of  the Genesee River basin.   The major mineral constituents  of  all
 samples were quartz,  illite,  and chlorite; quartz was predominant  at  all but
 the lowest flows.   The shale,  siltstone, and sandstone bedrock underlying  the
 basin  consist  predominantly of quartz; the till and glacial-lake deposits
 overlying  bedrock within the  basin are weathered and transported material
 derived mostly from the regional rocks.

     The  major clay constituents throughout the basin are illite and  chlorite.
 The  ratio  of illite to chlorite is consistent throughout the basin, with a
 mean value of  about 3.4:1.

     Most  sediment  samples consisted mainly of quartz and illite.  However,
 samples from Canaseraga Creek also contained substantial amounts of calcite,
which  is  probably derived from limestone sediments in the local glacial  drift
 in  the vicinity.
                                     1-15

-------
            TABLE 5.--MINERALOGICAL ANALYSES OF SEDIMENT MATERIAL,
                      GENESEE RIVER BASIN, 1975-77
SIZE MINERAL CONSTITUENT 4/
STATION I/ DATE TIME MATERIAL 2/ MM 3/ Q P K C CL IL CH KA
04218710 052975 — STREAM BED — 36 8 0 - 56
04218740 052975 — STREAM BED — 54 12 1 - 33
04218740 052975 — STREAM BED ' — 45 8 0 - 47
04218741' 052975 — STREAM BED — 37 9 0 - 54
04221000 071775 1030 STREAM BED <0.062 50 5 3 - 42
04221000 071775 — STREAM BED >0.062 35 10 - - 55
04221000 071775 1030 STREAM BED >0.062 81 4 3 - 12
04221000 071775 1030 STREAM BED >0.062 69 5 3 2 21
04221000 092675 1600 HIGH FLOW >0.062 68 16 3 - 13
04221000 092675 — HIGH FLOW <0.062 42 5 3 - 50
04221000 092675 — HIGH FLOW <0.062 45 6 7 7 35
04221000 100975 1630 SUSPENDED <0.062 45 6 3 - 46
04221000 121475 1020 STREAM BED <0.062 28 7 4 - 61
04221000 021776 1430 SUSPENDED <0.062 35 7 1 - 57
04221000 031376 0930 STREAM BED PSR 46 5 - - 49
04221000 031376 0930 STREAM BED <0.062 46 5 3 - 46
04221725 071775 — STREAM BED <0.062 28 6 - - 66
04221725 071775 -- STREAM BED >0.062 73 4 9 1 13
04221725 091275 1300 HIGH FLOW <.0062 45 5 - - 50
04221725 092675 1840 HIGH FLOW <.0062 53 5 - - 42
04221725 121475 1100 STREAM BED PSR 41 9 - - 50
04221725 020976 — LOW FLOW <0.062 38 6 3 4 49
I/ STATION NUMBER REFERS TO LOCATION IN FIGURE 1 AND TABLE 1
EXCEPT THE FOLLOWING SITES:
— .
— .
31
40
9
17
10
40
28
38
49
—
40
37
47
10
38
32
38
41



—
11
15
3
4
3
10
7
8
12
—
8
9
19
3
12
10
12
8


-
—
-
-
-
—
—
—
-
—
-
—
1
—
-
—
—
—
-
—


04218710 ERIE (BARGE) CANAL, AT GENESEE RIVER JUNCTION ENTRANCE,
AT ROCHESTER
04218740 ERIE(BARGE) CANAL, AT GENESEE RIVER JUNCTION EXIT,
AT ROCHESTER
04218741 ERIE(BARGE) CANAL, AT GENESEE RIVER JUNCTION
100 M FROM EXIT, AT ROCHESTER
04224000 MOUNT MORRIS LAKE NEAR MOUNT MORRIS


















04224964 LITTLE MILL CREEK, AT COUNTY LINE ROAD, NEAR DANSVILLE
04224965 LITTLE MILL CREEK RESERVOIR NEAR DANSVILLE
04227610 GENESEE RIVER, AT BIG TREE ROAD, NEAR GENESEO
04221400 GENESEE RIVER, AT ROCHESTER FIRE CLUB, ROCHESTER
04221500 GENESEE RIVER, ABOVE COURT STREET DAM, ROCHESTER












2/
3/
4/
CORE@ DENOTES DEPTH BELOW SURFACE, IN METERS
AUTOM S. DENOTES AUTOMATIC SUSPENDED-SEDIMENT  SAMPLER

PSR DENOTES PIPET PARTICLE-SIZE ANALYSIS RESIDUE
BWR DENOTES BOTTOM WITHDRAWAL PARTICLE-SIZE ANALYSIS RESIDUE
Q-QUARTZ      P-PLAGIOCLASE
CL-CLAY       IL-ILLITE
VALUES ARE IN PERCENT
K»K FELDSPAR
CH-CHLORITE

(continued)
C-CALCITE
KA-KAOLINITE
                                     1-16

-------
                            TABLE 5  (continued).
STATION If DATE
04221725
04221725
04221725
04221725
04221725
04221725
04221725
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04223000
04224000
04224000
04224000
021776
021876
031376
031376
040176
042476
100976
021975
071775
071775
091275
092675
092675
092675
111875
121475
012776
021776
021776
030476
031376
031376
031376
042276
042576
042576
102176
031077
031377
031377
031377
031377
031377
031377
031477
031477
033077
040377
042377
042377
042377
042477
072976
072976
072976
TIME
1230
1540
1100
1100
—
1450
1530
—
— -
1230
1350
1040
—
1435
1645
1230
1500
1350
1600
1610
1200
1200
1200
1330
1350
1905
0815
1640
0820
1030
1150
1525
1750
1910
0950
1825
1100
1340
1820
1820
1820
1220
—
—
™
SIZE
MATERIAL 2/ MM 3/
SUSPENDED
HIGH FLOW
STREAM BED
STREAM BED
LOW FLOW
LOW FLOW
HIGH FLOW
LOW FLOW
STREAM BED
STREAM BED
HIGH FLOW
HIGH FLOW
HIGH FLOW
HIGH FLOW
HIGH FLOW
STREAM BED
HIGH FLOW
HIGH FLOW
HIGH FLOW
RECESSION
STREAM BED
STREAM BED
STREAM BED
SUSPENDED
HIGH FLOW
SUSPENDED
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
CORE02.7M
CORE01.5M
CORE@1.2M
<0.062
<0.062
<0.062
<0.062
<0.062
—
<0.062
<0.062
<0.062
>0.062
—
>0.062
<0.062
<0.062
<0.062
PSR
—
—
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
__
PSR
PSR
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
PSR
—
~
~"~
MINERAL CONSTITUENT 4/
Q P K C CL IL CH KA
50 9
48 8
67 11
72 4
29 6
54 11
47 7
51 9
50 6
53 11
52 8
86 4
60 8
58 7
60 11
30 8
48 8
63 8
55 6
58 11
68 7
60 8
68 5
36 8
56 6
47 9
45 14
30 6
48 5
49 7
49 8
47 11
35 8
46 13
46 4
51 8
48 8
35 13
45 7
47 7
53 10
55 9
27 5
25 6
48 7
-
-
-
2
3
4
2
2
-
24
5
-
5
7
-
3
5
3
2
5
-
3
4
0
-
0
9
4
4
4
4
6
6
5
5
4
12
6
5
8
3
7
3
3
4
-
-
-
3
4
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
4
4
4
3
2
4
3
3
3
2
3
6
3
3
4
—
—
~
41
44
22
19
58
31
44
38
44
12
35
10
27
28
29
59
39
26
37
26
25
29
23
56
38
44
32
56
39
36
36
34
47
33
46
34
30
43
37
35
31
25
65
66
41
32
34
18
15
45
25
34
29
32
9
27
—
20
21
22
42
29
20
27
19
20
23
18
—
29
—
24
38
27
24
24
24
35
23
33
26
20
31
27
27
22
19
53
52
32
9
10
3
4
13
6
10
9
12
3
8
—
7
7
7
17
10
6
10
7
5
6
5
—
9
—
8
16
10
10
10
9
11
9
11
8
9
10
8
6
7
6
10
11
9
-
-
1
-
-
-
-
T 5/
-
-
-
-
-
-
-
T
-
-
-
-
T
-
-
-
-
-
T
2
2
2
2
1
1
1
2
-
T
2
2
2
2
T
2
3
T
5/  T - TRACE
                                 (continued)
                                     1-17

-------
TABLE 5  (continued).
STATION I/ DATE
04224000
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224848
04224848
04224848
04224848
04224848
04224900
04224930
04224940
04224940
04224940
04224940
04224940
04224964
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224978
04224978
04224978
04224978
04224978
04224978
04224978
04224978
072976
062675
072675
• 121375
021076
021176
021876
031276
042176
042576
052076
062476
081576
100976
042477
021176
021876
042576
072976
100976
032877
032877
072976
032877
032877
042377
042377
032877
082576
082576
082576
082576
082576
082576
082576
082576
082576
082576
082576
012776
021776
021776
021876
052076
072976
100976
032877
TIME .
--
1700
1700
1200
— -
—
1445
1330
—
1620
1200
1430
0515
1705
1630
—
0905
1130
1835
1615
1500
1440
1810
1500
1555
1915
1915
1720
—
— —
__
—
—
—
—
—
—
—
—
—
1525
1645
0930
—
1745
1555
1715
SIZE
MATERIAL 2/ MM 3/
SURFACE
STREAM BED
STREAMBED
STREAM BED
LOW FLOW
SUSPENDED
SUSPENDED
STREAM BED
LOW FLOW
HIGH FLOW
LOW FLOW
STREAM BED
AUTOM S.
HIGH FLOW
AUTOM S.
SUSPENDED
HIGH FLOW
HIGH FLOW
HIGH FLOW
HIGH FLOW
STREAM BED
STREAM BED
HIGH FLOW
SUSPENDED
STREAM BED
SUSPENDED
SUSPENDED
STREAM BED
CORE@1.5M
CORE@1.5M
CORES 1.5M
CORE@1.5M
CORE@2.3M
CORE02.3M
CORE@2.3M
CORE@6.4M
CORE(?6.4M
CORE@6.4M
CORE@6.4M
SUSPENDED
HIGH FLOW
HIGH FLOW
HIGH FLOW
LOW FLOW
HIGH FLOW
HIGH FLOW
SUSPENDED
—
<0.062
>0.062
PSR
<0.062
<0.062
<0.062
<0.062
<0.062
—
<0.062
<0.062
PSR
PSR
PSR
<0.062
<0.062
—
PSR
PSR
<0.062
<0.062
PSR
PSR
<0.062
<0.062
PSR
<0.062
<0.062
>0.062
<0.062
>0.062
<0.062
>0.062
<0.062
<0.062
>0.062
<0.062
>0.062
<0.062
<0.062
<0.062
<0.062
<0.062
PSR
PSR
<0.062
q
53
35
66
31
38
39
36
59
26
57
36
56
22
58
43
41
49
39
40
49
65
58
46
47
43
46
52
49
65
60
59
59
56
49
53
47
46
51
42
40
59
60
49
43
44
38
41
MINERAL CONSTITUENT 4/
P K C CL IL CH
9
19
6
6
12
8
4
9
5
14
7
6
6
6
4
9
13
8
6
7
-
10
8
12
11
28
4
10
5
11
7
7
9
5
7
9
6
5
13
11
8
7
12
12
12
12
5
4 -
_ _
- 8
2 8
5 4
1 -
1 -
4 7
4 4
3 3
3 -
- 17
- -
- 9
15 8
1 -
13 -
- _
5 1
3 -
8 -
4 3
4 7
4 17
5 15
2 10
17 8
8 5
3 1
5 -
4 -
5 -
_ —
3 -
4 -
_ _
3 -
e „
- i
3 -
4 4
6 3
4 -
4 8
5 5
5 9
5 10
34
46
20
53
41
52
59
21
61
23
54
21
72
27
30
49
25
53
48
41
27
25
35
20
26
14
19
28
26
24
30
29
35
43
36
44
45
39
44
46
25
24
35
33
34
36
39
27
33
13
38
30
—
—
16
47
18
39
16
59
21
23
—
18
40
36
30
20
18
26
14
16
10
13
18
19"
17
23
23
27
33
29
32
33
30
34
—
18
17
26
24
25
27
27
7
13
6
15
11
—
—
5
14
5
15
5
13
6
7
—
7
13
12
11
7
7
9
6
9
4
5
10
6
7
7
6
8
10
7
12
12
9
10
—
7
7
9
9
9
9
9
KA
T
-
1
-
-
-
-
-
-
-
-
-
T
-
T
-
-
-
-
-
T
-
-
T
1
-
1
-
1
—
-
-
-
-
-
—
-
—
-
-
—
-
-
-
-
-
3
(continued)




1-18








-------
TABLE 5  (continued).
STATION II DATE
04224978
04224978
04225000
04225000
04225000
04225000
04225000
04225000
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225600
04225600
04225670
04225670
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225950
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04227000
04227000
04227000
04227000
032877
042477
062675
062675
012776
021076
021776
021876
062375
072375
121375
021176
021776
030576
031276
042276
042476
042477
021876
102176
071775
042576


071975
071975
011476
020976
021776
030476
042377
011476


062675
062675
062675
121375
011476
021176
042276
062576
042377
062675
070875
071775
072375
TIME
1715
1425
1720
1720
—
—
1330
—
1930
1930
0900
--
1810
1215
0900
1330
1830
0910
1015
1105
—
1340
—
~
—
— -
--
—
1035
1600
2000
1410
—
—
— -
—
--
1550
1530
0900
0930
1045
1910
1915
1530
1915
1800
SIZE
MATERIAL 2/ MM 3/
STREAM BED
SUSPENDED
STREAM BED
STREAM BED
SUSPENDED
LOW FLOW
HIGH FLOW
SUSPENDED
STREAM BED
STREAMBED
STREAM BED
SUSPENDED
HIGH FLOW
RECESSION
STREAM BED
LOW FLOW
LOW FLOW
SUSPENDED
HIGH FLOW
SUSPENDED
STREAM BED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
SUSPENDED
LOW FLOW
HIGH FLOW
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
SUSPENDED
HIGH FLOW
LOW FLOW
STREAM BED
SUSPENDED
STREAM BED
LOW FLOW
STREAMBED
STREAMBED
<0.062
PSR
XJ.062
<0.062
<0.062
<0.062
—
PSR
<0.062
X0.062
PSR
PSR
--
—
<0.062
<0.062
_
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
>0.062
<0.062
<0.062
—
—
<0.062
<0.062
<0.062
<0.062
< 0.62
> .25
> .062
PSR
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
0.062
XJ.062
>0.062
q
39
42
66
48
36
42
56
43
34
59
46
37
66
54
56
40
59
40
54
28
44
28
52
45
34
59
26
51
51
48
47
24
40
42
56
50
63
27
33
58
30
67
38
34
23
58
55
MINERAL CONSTITUENT 4/
P K C CL IL CH KA
18
8
11
14
8
7
9
12
7
6
11
9
9
12
8
10
11
9
10
6
9
6
6
10
7
14
5
5
8
12
9
5
23
8
7
22
13
5
6
8
7
14
9
12
6
7
9
2 18
6 12
- 7
- -
1 -
4 2
3 5
4 -
- -
5 11
4 4
4 -
- -
6 -
- -
3 3
- -
4 12
5 -
- -
3 3
3 -
3 8
3 12
4 -
8 3
3 -
3 -
4 -
7 -
8 6
2 -
3 2
7 12
- 3
4 4
- 4
- 5
1 -
4 -
- 5
3 -
5 9
15 6
- 9
- 12
4 9
23
32
16
38
55
45
27
41
59
19
35
50
25
28
36
44
30
35
31
66
41
63
31
30
55
16
66
41
37
33
30
69
32
31
34
20
20
63
60
30
58
16
39
33
62
23
23
17
22
12
27
—
34
20
—
43
14
27
—
19
21
30
35
23
25
21
48
30
—
23
22
39
11
—
31
27
25
22
__
23
22
26
15
14
47
— —
21
43
12
30
24
46
15
15
6
9
4
11
—
11
7
—
16
5
8
—
6
7
6
9
7
9
10
18
11
—
7
7
16
5
—
10
10
8
7
—
7
8
8
5
6
16
__
9
15
4
8
9
16
5
8
-
1
„
-
-
-
-
-
-
-
-
-
-
-
-
-
_
1
-
-
-
-
1
1
-
T
-
—
—
—
1
-
T
1
—
_
—
T
—
_
-
_
1

_
3
T
(continued)




1-19








-------
TABLE 5  (continued),
STATION I/ DATE
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227500
04227610
04227610
04227610
04227610
04227610
04228500
04228500
04228500
04228500
04228500
04228500
092675
092675
121375
. 011376
021976
031276
042576
102176
042377
042477
042577
062775
062775
062775
062775
070975
082675
082675
082775
082775
082775
082775
092675
121475
011376
021976
030476
030476
031376
031376
042576
102176
112776
033077
042477
082875
082875
082875
082875
082875
070975
071775
071975
092775
120275
121475
TIME
1040
1515
1615
—
0930
1600
1430
1230
1245
1050
0900
—
—
—
—
1115
—
—
—
—
—
—
1600
1345
—
1220
1450
1750
1345
1345
2015
1140
1105
1340
1208
~
—
—
~
—
0830
1445
1445
0915
—
1500
SIZE
MATERIAL 2/ MM 3/
HIGH FLOW
HIGH FLOW
STREAM BED
LOW FLOW
HIGH STAGE
STREAM BED
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
LOW FLOW
STREAM BED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
HIGH FLOW
STREAM BED
LOW FLOW
RECESSION
HIGH FLOW
HIGH FLOW
STREAM BED
STREAM BED
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
LOW FLOW
STREAMBED
STREAM BED
HIGH FLOW
SING-STAGE
STREAM BED
<0.062
<0.062
PSR
—
<0.062
PSR
—
PSR
<0.062
<0.062
<0.062
> 4
> 0.25
> .062
< .062
0.062
__
—
—
—
—
—
<0.062
PSR
— .
—
<0.062
<0.062
<0.062
PSR
-—
PSR
PSR
PSR
PSR
—
— -
—
—
—
0.062
>0.062
>0.062
<0.062
<0.062
PSR
Q
56
54
43
31
48
26
45
52
44
34
42
47
44
61
40
24
51
49
53
41
29
40
60
59
49
48
55
50
61
40
53
45
55
46
38
42
50
41-
32
38
36
34
63
56
73
37
MINERAL CONSTITUENT 4/
P K C CL IL CH KA
8
10
7
8
9
8
9
8
17
21
17
4
7
14
5
5
11
10
12
7
7
8
10
12
9
8
12
11
6
6
8
10
6
9
6
9
10
* 8
5
7
10
2
10
11
10
7
7
—
—
5
11
7
8
—
4
3
6
17
36
5
2
—
1
2
0
0
2
3
—
—
3
4
—
3
4
5
3
3
—
3
9
0
1
1 *
1
1
—
7
5
—
—
-
-
~
3
-
2
-
..
4
3
9
5
6
—
-.
2
—
-.
—
-
—
~
_
—
—
-
8
—
—
—
—
—
3
—
3
13
_
—
—
_
—
5
4
3
—
—
-
29
36
47
56
30
59
38
36
32
33
30
26
13
20
51
71
37
39
35
52
62
50
30
29
39
32
33
36
29
49
36
39
39
39
34
49
39
50
62
54
49
53
19
33
27
56
21
27
36
38
22
47
29
29
22
23
19
20
10
13
37
55
—
—
— —
—
— —
—
22
22
29
25
24
27
25
41
27
29
30
28
26
__
— _
—
__
— —
36
37
15
25
20
41
8
9
11
18
8
10
9
7
8
8
9
6
3
7
14
16
—
__
—
__
—
—
8
7
10
7
9
9
7
8
9
10
9
9
8
__
—
__
__
—
13
13
4
8
7
13
-
_
_
_
_
2
_
_
2
2
2
_
—
_
_
_
_
_
_
_
_
_
_
_
_
_
_
_
_
_
_
_
—
2
T
_
_
_
_
_
_
3
T
_
_
2
     (continued)
         1-20

-------
TABLE 5  (continued).
STATION 11 DATE
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04228500
04230380
04230380
04230380
04230380
04230380
04230380
04230380
04230380
04230410
04230500
04230500
04230500
04230500
04230500
04230500
04230500
04231000
04231000
04231000
04231000
04231000
04231400
04231500
04232000
04232000
04232000
04232000
04232000
04232000
04232000
121975
011476
021076
021776
022476
030476
031376
031376
031376
042676
073176
110176
030977
042477
042877
042977
071875
071875
121575
021176
030376
031476
042776
052076
021176
071875
071875
121575
021276
030576
031476
042676
071875
071875
121575
031476
042676
052975
052975
070975
011476
021276
021976
021976
030476
042376
TIME
1100
—
—
1500
1645
1900
1500
1500
1500
1805
1255
0905
1050
1655
1510
1145
0915
0915
0930
—
1650
0945
1015
0930
—
1200
1200
— -
--
1345
1430
1200
1240
1240
—
1350
1545
—
~
1430
--
__
1700
0800
1200
1030
SIZE
MATERIAL 2/ MM 3/
RECESSION
LOW FLOW
LOW FLOW
HIGH FLOW
HIGH FLOW
HIGH FLOW
STREAM BED
STREAM BED
STREAM BED
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
STREAM BED
LOW FLOW
HIGH FLOW
STREAM BED
LOW FLOW
RECESSION
LOW FLOW
STREAM BED
STREAMBED
STREAM BED
LOW FLOW
HIGH FLOW
STREAM BED
SUSPENDED
STREAM BED
STREAMBED
STREAMBED
STREAM BED
SUSPENDED
STREAM BED
STREAM BED
LOW FLOW
LOW FLOW
LOW FLOW
HIGH FLOW
HIGH FLOW
RECESSION
SUSPENDED
<0.062
—
<0.062
<0.062
—
0.062
<0.062
<0.062
<0.062
BWR
PSR
PSR
PSR
<0.062
PSR
<0.062
>0.062
<0.062
<0.062
<0.062
PSR
<0.062
<0.062
BWR
<0.062
<0.062
>0.062
PSR
<0.062
BWR
PSR
<0.062
<0.062
>0.062
PSR
PSR
<0.062
--
—
0.062
_
<0.062
<0.062
<0.062
<0.062
<0.062
Q
40
47
27
56
38
45
56
71
57
45
48
41
43
43
48
41
61
34
32
43
54
54
35
45
30
26
29
38
37
34
44
31
20
29
31
40
16
46
46
26
—
46
47
58
53
31
MINERAL CONSTITUENT 4/
P K C CL IL CH KA
22
9
9
11
21
10
7
4
6
6
8
9
20
8
6
7
6
7
5
8
11
7
5
6
6
9
7
5
3
5
5
4
7
11
6
7
3
8
8
4
_
9
24
7
8
5
- 3
- -
4 -
4 -
- -
5 -
3 4
3 -
5 6
9 -
— -
5 -
4 -
3 8
4 6
7 3
5 4
- 6
4 11
4 -
- -
4 8
3 -
- -
3 -
- 25
6 51
3 15
— —
4 2
2 24
- 7
- 11
6 37
3 18
6 8
2 -
1 -
1 -
- 4
_ _
3 -
— —
4 -
4 -
- -
35
44
60
29
41
40
30
22
26
40
44
45
33
38
36
42
24
53
48
45
35
27
57
49
61
40
7
39
60
55
25
58
62
17
42
39
79
45
45
66
__
42
29
31
35
64
24
32
47
21
31
31
24
18
21
31
34
35
23
28
27
29
18
40
34
33
26
21
42
36
50
31
5
30
47
43
20
48
56
14
31
31
— _
__
—
51
__
32
21
22
26
51
11
12
11
8
10
9
6
4
5
9
10
10
8
9
7
11
6
13
14
12
9
6
15
13
11
9
2
7
10
12
4
10
6
3
10
8
—
__
__
15
_—
9
8
9
9
13
-
-
2
-
-
-
-
-
T
-
—
T
2
1
2
2
—
_
—
-
—
—
—
—
T
—
—
2
3
—
1
T
—
-
1
-
_
_
_
_
__
1
_
_
_
-
     (continued)
        1-21

-------
                            TABLE 5   (continued).
LOCATION 6/
CLAY BED RD, FILLMORE
CLAY BED RD, FILLMORE
EMO RD, S. OF PATCHINVILLE
EMO RD, S. OF PATCHINVILLE
ESTERBROOK FARM, HOUGTON
ESTERBROOK FARM, HOUGTON
GRAHAM FARM, N. , PORTAGEVIL
GRAHAM FARM, N. , PORTAGEVIL
GRAHAM FARM, N. , PORTAGEVIL
GRAHAM FARM, N. , PORTAGEVIL
GRAHAM FARM, N. , PORTAGEVIL
GRAHAM FARM, N. .PORTAGEVIL
GRAHAM FARM, S. , PORTAGEVIL
GRAHAM FARM, S. .PORTAGEVIL
GRAHAM FARM, S. , PORTAGEVIL
WEARKLEY RD, NR PATCHINVIL
LATTICE BR RD, HOUGTON
MILL CR RAVINE, PERKINSVIL
MILL CR RAVINE, PERKINSVIL
RT 36, DANSVILLE
RT 63, DANSVILLE
RT 63, 1.4 KM E.OF DANSVIL
RT 63, 1.4 KM E.OF DANSVIL
SHONGO CR. BR, CANEADEA
DATE
073076
073076
051376
051376
073076
073076
120876
120876
120876
120876
120876
120876
120876
120876
120876
062277
073076
040276
040276
040276
040276
051376
051376
073076
MATERIAL
LCS
LCS
HLD TILL
HLD TILL
AN
TG
AN
LCS
TG
AF
AF
AF
L
AN
AF
HLD TILL
LCS
LCS
TBS
TILL
V.CLAY
BR LAKE
BR LAKE
AF
SIZE
11 MM
<0.062
<0.062
<0.062
X).062
<0.062
<0.062
—
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
>0.062
<0.062
Q
16
22
72
66
52
51
—
34
40
62
16
44
34
61
48
38
42
51
44
33
45
52
56
50
MINERAL CONSTITUENT
P K C CL IL CH
6
6
5
5
6
6


6
8
6
4
6
7
9
6
7
8
15
7
8
11
10
7
6
4
3
4
3
-
-


3
3
2
-
4
4
4
2
4
3
3
4
5
5
8
-
4
-
3
1
-
-
-


4
4
7
18
-
-
-
-
7
-
16
16
29
13
2
3
—
74
66
18
26
42
43


53
45
23
62
46
55
26
44
44
47
15
29
25
26
28
34
40
64
55
15
22
37
34


42
36
19
56
40
45
23
40
37
40
9
22
18
17
22
29
32
10
11
3
4
5
8
—
11
9
4
6
6
10
3
4
7
7
5
7
7
8
6
5
8
KA
—
—
—
—
— •
1
—
—
T
—
—
—
—
—
—
TR
—
1
—
TR
1
—
—
—
6/ GRAHAM FARM, N. DENOTES NORTHERN  PART  OF  SLIDE AREA,  GENESEE RIVER,
      3 KM SOUTH OF PORTAGEVILLE
   GRAHAM FARM, S. DENOTES SOUTHERN  PART  OF  SLIDE AREA,  GENESEE RIVER,
      3 KM SOUTH OF PORTAGEVILLE
   BR DENOTES BRIDGE
   CR DENOTES CREEK
   E  DENOTES EAST
   RD DENOTES ROAD

7/ AF       DENOTES ALLUVIUM ABOVE 100-YEAR  FLOOD LEVEL
   AN       DENOTES ALLUVIUM BELOW 100-YEAR  FLOOD LEVEL
            (MULLER, YOUNG, RHODES,  WILLETTE,  WILSON,
               1976, NEW YORK  STATE  GEOLOGICAL SURVEY, WRITTEN COMMUN.)
   HLD TILL DENOTES HIGHLAND SANDY TILL
   L        DENOTES GLACIAL LAKE  MATERIAL
   LCS      DENOTES LACUSTRINE SILT  AND CLAY
   TBS      DENOTES BROWN SANDY TILL
   TG       DENOTES DENSE GRAY TILL
   V.CLAY   DENOTES VARVED CLAY
   BR LAKE  DENOTES BROWN GLACIAL LAKE  MATERIAL
                                     1-22

-------
STREAMFLOW- AND SUSPENDED-SEDIMENT-DURATION ANALYSES

     Streamflow- and suspended-sediment-duration curves depict the temporal
distribution of mean daily  data  at  a given location.  Ten such curves are pre-
sented in figure 4.  Where  streamflow data are available from stations
operated before this study  (see  table 1),  analyses of these data are presented
for comparison with the June  1975 to May 1977 data.   The curves illustrate
that high streamflows, high suspended-sediment concentration, and high sedi-
ment loads occurred during  only  a small percentage of time during the study.
For example, sediment  in  amounts greater than 10,000 Mg per day was
transported by the Cenesee  River at Rochester only 12 percent of the time
during 1975-77.

     Another application  of duration curves is to determine the percentage of
time that a particular concentration value was equaled or exceeded.  For
example, from June 1975 to  May 1977, the median stream discharge (equaled or
exceeded 50 percent of the  time) of the Genesee River at Rochester (fig. 4J)
was 60 m^/s.  Median suspended-sediment concentration was 40 milligrams per
liter, and median suspended-sediment discharge was 200 Mg per day.
SUSPENDED-SEDIMENT YIELD

     Duration  curves  can  "be  used to compute the average annual suspended-
sediment yield at sampling stations.   Sediment yields during this study were
determined by  the transport-duration technique described by Miller (1951),
which uses sediment-transport  curves and streamflow-duration curves such as
those presented in figure 4.   An example of the computational procedure to
determine average annual  suspended-sediment load and yield at Rochester is
given in table 6.  Two  assumptions are made in this method:  (1) that the
sediment-transport and  flow-duration curves represent long-term relationships,
and (2) that the observed instantaneous suspended-sediment discharge has the
same relation  to the  corresponding water discharge as mean daily sediment has
to water discharge.   The  advantage of this method is that, within these
assumptions, a computation can be made from only a few years of streamflow
and(or) sediment discharge.

     Calculated average annual suspended-sediment yields for stations with
daily streamflow records  are  given in table 7.  The values shown for the
Genesee River  at Wellsville,  Canaseraga Creek at Shakers Crossing, Oatka Creek
at Warsaw and  Garbutt,  and Black Creek at Churchville are lower than antici-
pated from field observations  and areal study.  Although the values in table 7
are valid within the  accuracy  of the technique used to obtain them, values
about twice those listed  for  the sites may be more realistic.
                                    1-23

-------
     TABLE 6.  COMPUTED AVERAGE ANNUAL SUSPENDED-SEDIMENT  LOAD  AND
               YIELD, GENESEE RIVER AT ROCHESTER,  BASED  ON 1953-77
               STREAMFLOW AND 1975-77 SEDIMENT WATER-YEAR  RECORDS

(1) .
Percentage
of time
discharge
was equaled
or exceeded
0.0-0.25
0.25-0.75
0.75-1.5
1.5-2.5
2.5-4.5
4.5-8.5
8.5-15
15-25
25-35
35-45
45-55
55-75
75-95
95-100
Totals
(2)

Interval
(percentage
time of
column 1)
0.25
.50
.75
1.0
2
4
6.5
10
10
10
10
20
20
5
100
(3)

Mld-
ordinate
(percent of
column 2)
0.125
.50
1.125
2.0
3.5
6.5
11.75
20
30
40
50
65
85
97.5

(4)


Water
discharge
(m3/s)
540
435
380
340
297
260
180
120
84
62
46
30
18
13

(5)

Suspended-
sediment
discharge
(megagrams/day)
56,000
29,000
21,000
15,500
11,000
7,800
3,200
1,320
650
365
220
110
55
35

(6)
Average
daily sedi-
ment discharge
(column 2 x
column 5)
140
145
158
155
220
312
208
132
65.0
36.5
22.0
22.0
11.0
1.8
1,628
Average annual suspended-sediment load
  (1,628 Mg/d x 365 days)	
Average annual suspended-sediment yield
  (594,000 Mg / 6.364 km).....	
.594,000 Mg


..93  Mg/km2.
                                    1-24

-------
TABLE 7.  DRAINAGE AREA AND AVERAGE ANNUAL SUSPENDED-SEDIMENT LOAD AND
          YIELD AT STATIONS SAMPLED IN GENESEE RIVER BASIN


04221000
04221725

04222300
04223000
04224740
04224775
04224848

04224900
04224930
04224940
04222978
04225000
04225500
04225600.
04225670
04225915
04225950
04226000
04227000

04227500
04228500
04230320
04230380
04230400
04230410
04230423
04230470
04230500
04231000
04232000
Station number and name
Genesee River at Wellsville
Genesee River at Transit Bridge
near Angelica
Genesee River near Houghton
Genesee River at Portageville
Sugar Creek near Canaseraga
Canaseraga Creek above Dansville
Stony Brook at Stony Brook
State Park
Mill Creek -at Patchinville
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Canaseraga Creek near Dansville
Canaseraga Creek at Groveland
Bradner Creek near Dansville
Bradner Creek near Sonyea
Keshequa Creek at Nunda
Keshequa Creek at Tuscarora
Keshequa Creek at Sonyea
Canaseraga Creek at Shakers
Crossing
Genesee River near Mount Morris
Genesee River at Avon
Oatka Creek at Rock Glen
Oatka Creek at Warsaw
Oatka Creek at Pearl Creek
Pearl Creek at Pearl Creek
Oatka Creek near Pavillion Center
Mad Creek near Le Roy
Oatka Creek at Garbutt
Black Creek at Churchville
Genesee River at Rochester
Drainage
area
(kift2)
749

1,494
1,940
2,541
49.7
233

53.9
13.0
46.9
57.0
93.0
396
469
19.3
106
84.4
152
178

862
3,670
4,318
41.4
109
209
28.2
288
26.2
528
319
6,364
Measured
average annual
suspended-
sediment load
(1976-77)
(Ms)
44,000

—
—
1,080,000
—
—

—
—
_
_
—
—
—
—
—
—
—
_

222,000
990,000
794,000
_
_
__
_
__
_
10,900
«.
1,060,000
Calculated
average annual
suspended-
sediment load
(1975-77)
(Mg)
81,300

—
—
540,000
—
28,600

__
—
__
__
—
—
—
—
—
—
__
44,000

144,000
1,390,000
949,000
«.
3,660

_..
_—
—,
6,260
»
594,000
Suspended-
sediment
yield
(1975-77)
(Mg/km2)
108

—
—
212
__
123

_-
__
__
__
__
__
__
__
__
__
__
247

167
378
220

34

»
_—
«—
12

93
                              1-25

-------
                                    SECTION  6

                  DISCUSSION OF  SUSPENDED-SEDIMENT DISCHARGE

     Records and curves  of  suspended-sediment  concentration and suspended-
sediment-discharge duration show that  high  streamflow,  high suspended-sediment
concentration, and high  suspended-sediment  discharge occurred during only a
small percentage of  time from  1975-77,  but  the total amount of suspended-
sediment transported during the  small  time  percentage was relatively large.
Conversely, streamflow and  suspended-sediment  discharge were low during a
large percentage of  time, and  the total amount of suspended-sediment
transported at low flows was relatively small.

     From April 1975 to  September 1977, the greatest daily suspended-sediment
load transported by  the  Genesee  River  (201,000 Mg) was at Portageville on
February 17, 1976.   This load  represents 19 percent of the total measured at
that station during  the  1976 water year.  From February 16-20, 1976, the
Genesee River  at Portageville  transported a sediment yield of 197 Mg/km2—
seven times the yield at Wellsville (28 Mg/km2) and 5 1/2 times that at
Rochester  (35  Mg/km2).   The suspended-sediment load transported past the
Wellsville and Portageville sampling stations  during February 1976 was 62 per-
cent of the amount transported during  the 1976 water year.  During February
1976, streamflow at  Wellsville and Portageville was 27 percent, respectively,
of  the annual  total; the large sediment load transported at that time is
attributed to  thawing and major  runoff after a winter freeze.

     The greatest monthly load at all  daily suspended-sediment stations during
the 1977 water year  was  in September.   The September totals represent from 1/4
to  1/2 of  the  annual loads  transported past the stations.  The second highest
amount was during March, when  about 20 percent of the annual load was
transported past most stations.

     The 1976  and  1977  annual  suspended-sediment  loads were about the same at
Portageville  as  at Rochester.   The totals at Wellsville, Canaseraga Creek  at
Shakers Crossing,  and Genesee  River near Mount Morris and at Avon were greater
in  1977 than  in  1976; however, the total for Oatka  Creek at Garbutt was
greater in 1976.   This  anomaly has not yet been explained.

     The amount  of sediment being deposited above the Mount Morris  dam is
undetermined.  Canaseraga Creek adds sediment to  the Genesee River  near Mount
Morris station,  and  deposition occurs in downstream river channels  wherever
gradients  are  low.   Some temporary deposition is  suggested  by  the downstream
suspended-sediment discharge progression.
                                     1-26

-------
     The greatest monthly  total  suspended-sediment yield during 1976-77 was In
the Genesee River at Portageville  (262 Mg/kra2 in February 1976) and in
Canaseraga Creek at Shakers  Crossing  (109 Mg/km2 in September 1977).  The
yield measured at Avon  was less  than  at Mount Morris; this reflects the normal
pattern of decreasing sediment yield  with increasing drainage area.  The
highest monthly yield during June-August 1976 was In July in the Genesee River
at Mount Morris (7.3 Mg/km2) and Portageville (7.2 Mg/km2).  Downstream from
Portageville, the month of highest yield was August, with 6.4 Mg/km2 at Avon
and 4.4 Mg/km2 at Rochester. This yield pattern suggests that under summer
hydrologic conditions,  sediment  is stored on the wide flood plains and in low-
gradient channels downstream from  Geneseo and Avon.

     Sediment load during  September 1977 was considerably less at the site
near Mount Morris than  at  Portageville, even with the inclusion of sediment
from Canaseraga Creek into the Genesee main stem, presumably because of con-
siderable sediment deposition in the  reservoir behind the Mount Morris dam.
However, without extensive cliraatological and hydrologic analysis, the low
sediment load between Portageville and Mount Morris cannot be fully explained.

     Results of particle-size analyses show that, in general, the percentage
of stream-transported sand is directly related to stream gradient, source
rocks, and unconsolidated  deposits.  Most of the source materials are at the
higher elevation within the  basin, where stream gradients are also the steep-
est.  Comparison of percentages  of sand-sized material at different sites show
a downstream decrease in sand percentage.
                                    1-27

-------
                                REFERENCES
Colby, B. R.  1956.  Relationship of sediment discharge  to  streamflow.  U.S.
     Geological Survey open-file report,  170 p.

Guy, H. P.  1969.  Laboratory theory and  methods for  sediment  analysis.   U.S.
     Geological Survey Techniques of Water Resources  Investigations, Book 5,
     Chapter Cl, 58 p.

Mansue, L. J., Young, R. A., and Soren, J.  1983.  Part  IIj Hydrogeologic
     influences on sediment transport patterns in  the Genesee  River basin.
     In Volume 4;  Streamflow and sediment transport, Final Report Genesee
     River Watershed.  U.S. Environmental Protection  Agency.

Miller, C. R.  1951.  Analysis of flow-duration sediment-rating method  of
     computing sediment yield.  U.S. Bureau of Reclamation, 55 p.

Porterfield, George,  1972,  Computation  of fluvial-sediment  discharge:   U.S.
     Geological Survey Techniques of Water-Resources  Investigations,  Book 3,
     Chapter C3, 66 p.

Walling,  D. E., 1976, Natural and channel erosion  of  unconsolidated source
     material (geomorphic control, magnitude and frequency  of  transfer
     mechanisms), in  Shear, H., and Watson, A. E.  P., eds., Proceedings,
     Workshop on the  fluvial transport  of sediment-associated  nutrients
     and  contaminants:  Kitchener, Ontario, International Joint  Committee
     Research Advisory Board, p. 1-36.

[U.S.] Water Resources Council, 1975, Instruments  and reports  for  fluvial
     sediment investigations, Catalog:  Federal Inter-Agency Sedimentation
     Project, Sedimentation Committee,  61 p.

Wolman, M. G., 1954,  A method of sampling coarse river-bed  material:  Trans-
     actions of the American Geophysical  Union, v. 35, no.  6,  p. 951-956.
                                   1-28

-------
                          7B-30'
                                                    78"
43'
42
30'
42
             EXPLANATION

 ,04227500 Stage and daily sediment
           ' site and number

£04231000 Stage-recording and sediment
           partial-record site and number

A04230470 Stage and sediment partial-
           record site and number

    O     Precipitation-recording site

  •*—3.4   Radiocarbon dating sample
           site and number!s) of samplels):
           tip of arrowhead is approximate
           site(s) location

  •—•— Drainage boundary          042304C
                                                                           77-30'
                                                                     LAKC ONTARIO
                   1O
                             20MILES
               10    20KILOMETERS
   Base from U.S. Goologiral Survttv
   NY .mil PA Si.n.. li.i-.i	MIS. I r.oo.
-------
                                         OC-I
     (M
      m
MOO
333
CO rtOO

H- M rt
re  -O  a
•  1
   n  a>
cu  n  <
3  H- CD
O.T3  1
   H. CO
*J rt 00
O  0>  (0
n  rt
3* H. a
(BOO
CO  3  3
rt     rt
CD  M> 3*
1  I  M
 o> ra
 3 n
 c P-
 CU T3

•^ rt
   to
 h-> rt
 VO H-
 ~J O
 Oi 3

 cn MI
 CD o
•a i
 rt
 fD -O

 S. ">
 cf i
 (B H-
 •^ o
   a.

 vO O
   B)  (D
   rt  n
   CD IX
   CO H->

   < VO
   H- *-
   (B -»J
  •  o
     CO
     3
     Cu
     s    §    s    s
                     ai
                     O
          8
^^

mini
                               MONTHLY TOTAL PRECIPITATION, IN MILLIMETERS

                                                      -•   —   N)

                                            00808         o    i
                                                                                       s
                                               unnnni
                              ,1(111)1)111
                                                   ill
                                                   ^»w
  MONTHLY TOTAL PRECIPITATION, IN MILLIMETERS
 *^                        -•    -*    ISJ

 S              00808          o

""                           '  '   '  'S         ""
               I


               M
               3
                                                                   S
                                                                                            M



                                                                                            I
                                                                                            
-------
•b.
                  0(331000 - tCNCSCC DlVCIt HI NCLL3«!UC, «. I.
                                                    MRTDt 7CMt
                                                o-tsre HRicit irw
                                                • - an UBTOI im»
 'lO'
               10'             10*            10'
                 NOTCH OI9CMMC, IH CUBIC ICtOIS PT" KCONO
                                                                  r
                                                                                         «- vxtu. »I«CT in iwwsn • IMC icm flNeeuw, H.I.
                                                                          B
ID1             10'             10'
  mien oiscHHwe, IN CUBIC MCTCTS m> straw
       Figure 3.—Instantaneous  streamflow and  suspended-sediment curves  for Genesee River basin:

                    A, Genesee River at  Wellsville;  B, Genesee River at  Transit  Bridge near Angelica.

-------
     s-
     E
     I
•-»   5
      ~\tf
                        04222300 - CCNCSCC RIVIII fCffi HOUEHTON, H.I.
                     10'             10'            10'
                       MHO* oisctwtec, IN CUBIC mwa rcn stcwc
                                                              10'
                                                                           i •
                                                                                            041311100 - CCNCJCC RIVE* BT PCHIIBttVILlC, ». I.
10'             10'             10'
  «BTW 015CHWW, IN CUBIC ICTTKS ft' STOJC
         Figure 3  (cont.).—Instantaneous streamflow and suspended-sediment  curves for Genesee  River  basin:

                                C, Genesee River near Houghton;  D,  Genesee River at Portageville.

-------
                      wow turn; xrm oMMcmtoi, n. i.
                                                                V
l"
             Itf            IQ'           10'
               MIDI OUCHWSC, IN CUBIC ICtOW fCR 9CGON9
                                                     10'
                                                                                 o«»«r?j - tuna.*** wctr iwwe OWSHLLC, «. r.
                                                                 i "
                                                                                 mm OIJCMMC. m CUBIC nciws PCH attm
                                                                                                         ID1
  Figure  3  (cont.).—Instantaneous streamflow and  suspended-sediment  curves  for Genesee River basin:
                        E, Sugar Creek near Canaseraga;  F, Canaseraga Creek above Dansvilie.

-------
     •o.
V   =
U)
                       0«n
-------
'    *
fc.\   ft


Ui   I
                           - HILL OWMC «T PDK1WHUC, K.T.
                    \
-------
u   £
     *
                            - ma trac ff omuv.'LLr, i.
       10'
             K
                    10'            10'  	        10'
                       wit* oiscwrcr, IN CUBIC nno« fr* xcoxo
                                                             10'
                                                                                          0431SSOO - otmsninefl CHECK «t cmwcLmD, N. t.
10*            10'

  WITCT OIlCHRRtC, IN CUBIC ICTCK) fFK
        Figure  3 (cont.).—Instantaneous  streamflow  and suspended-sediment  curves  for Genesee River basin:

                              K, Mill Creek  at Dansville; L,  Canaseraga  Creek  at Groveland.

-------
u>
VJ
                                                                        •o.
                             amocK wren mm nmsviac, H.I.
             M
                                                                        t,.
                                                                       -V


                                                                       S
                    10'            10*            10'
                       NOTtX OUCWWC, IN CUBIC ICITO PCX JCOKI
10-
                  N
                                                                                         Q423567Q * BRflDCR CHECK NCflR 9QNTCR/ N.T.
                                                                                                 I  »
                           10"            10*            10'
                             «m oncmrec, m CUBIC rerun t» xmo
         Figure  3 (cont.)-—Instantaneous  streamflow and suspended-sediment curves for Genesee River basin:

                              M,  Bradner Creek near Dansville;  N, Bradner Creek near Sonyea.

-------
00
      •b
                        OUU*1S - KMHCDUt OIKK RT NUHOT, N.I.
        10'
in'             10'            10"
  •IKK OIMMMC, IN CUBIC IC1CK3 fCK 9CCOND
                                                              10'
                                                                                            04135JM - KCJNtOUII CICCK RT 7U3OWOW1, N.T.
                                                                           10'
10'             10'             10'
  me* DIKMMO:, IN CUBIC icTcn mt XCCND
         Figure  3  (cont.).—Instantaneous  streamflow and  suspended-sediment curves  for Genesee River basin:

                                0,  Keshequa Creek  at Nunda; P,  Keshequa Creek at Tuscarora.

-------
                ouwxn - «I:JHEQUB wxx m emit touwi JOHICT, H.I.
                           10'            ID1
                        :, m CUBIC man re* SCCOND
                                                                                       awnsmncn CKCCK HT MKcm cmjsiNt. N.T.
'ID'
             10"
                           10'       _  10'
                    9CWHK, IN CUBIC HL1CRS fCM liv^Ml
                                                     10'
Figure 3  (cont.).—Instantaneous  streanflow and suspended-sediment curves for Genesee  River  basin:

                      Q, Keshequa Creek at  Craig Colony,  Sonyea; R,  Canaseraga Creek at Shakers Crossing.

-------
M   S


S   I
                        (HW75QQ - ttHESCC RIVCP NT  H3UNT IttWIS, * T.
                                                                         o.
       'id-
10'             10*            10*
  MICH oisowmc, IM CUBIC ictnts TR XCOND
                                                              10'
                                                                                                - celeste mvcR RT WON,
10'             10'            10'
  MHTCP oiscHnmc, IN CUBIC ncTnis IT* SCCOND
         Figure  3  (cont.).—Instantaneous  streamflow and suspended-sediment  curves for Genesee River  basin:

                                S,  Genesee River near Mount Morris;  T, Genesee River  at Avon.

-------
                     - ami went m raw aw, «, r.
      u
'10'
10''            Id"            10'
  •ncK Dimme, i* CUBIC ncms PCK SCOONQ
                                                     ib1
                                                                                 047W3M - OKIKR CHECK RT NNI9MI.
                                                                               10'            10'            10'
                                                                                 wrtCT aiJMMC. IN CUBIC ncTots m KCOND
 Figure  3 (cont.).—Instantaneous  streamflow and suspended-sediment  curves for Genesee  River  basin:

                       U,  Oatka  Creek at Rock Glen;  V, Oatka Creek at Warsaw.

-------
V
      v
                       oino4ia - KWL CHECK or nm meat, N.I.
             W
       I -•
ft-       	'ib*.'_.   	'ib'
  •not onatiwc, IN ante man mt sccao
                                                            10'
                                                                                               omicn turn nrmt NWILJIM conw, x. i.
                                                                         'i -
                                                                                      uf            10'            10'
                                                                                        MTCR OUCHOC, IN CUBIC HC1DO RR 3CCOND
                                                                                                                              10'
        Figure  3 (cont.)-—Instantaneous streamflow  and suspended-sediment curves  for Genesee River basin:

                               W, Pearl Creek at Pearl Creek; X, Oatka Creek near  Pavillion Center.

-------
      "a.
      -o.
l"1    e


»    I
<->    8
                           - 1*0 cat!* tew LC HOT, N.I.
                    10'            10'            10'
                      irart oncmtec, in CUBIC icmn PT» stcwn
                                                           10'
                                                                                             onicn cum m snuiiu'''!. « r
                                                                                     10'
10'
runic
        Figure 3  (cont.).—Instantaneous streamflow  and suspended-sediment curves for  Genesee River  basin:

                              Y, Mad Creek near LeRoy;  Z, Oatka Creek at Garbutt.

-------
                                          0011000 - ttNCJK HIVCR m ROCHTJtn, ». I.
                                 AA
                                        10'            10*
                                          MBTCT D13CHWCC, IN CUBIC ICTCKS PCK 9CCOND
                                                                              10'
Figure  3 (cont.).—Instantaneous streamflow and suspended-sediment curves for Genesee River  basin:
                     AA, Genesee River at  Rochester.

-------
10,000
 1000
  100
   10
   0.1
                                         i  r
         i  i  i   I   i
j	I
i   i  i   i  i  i
j	i
i  I  i  I
   ••.01  0.060.10.2 0.6  %  2   6  10   2O  30  40 50  60 70 80   90  85  98 9999.699.899.9   99.99
            PERCENTAGE OF TIME STREAMFLOW, SUSPENDED-SEDIMENT CONCENTRATION,
              AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED

Figure  4A.   Long-term  daily  streamflow and  June 1975-May  1977 mean daily
             btreamflow,  suspended sediment  concentration, and suspended
             sediment discharge, Genesee River at Wellsville.
                                   1-45

-------
    100,000
     10,000
  E >-
  -I <
o-
 i —rn  1000
    ir
    <
II
       100
    85
        10
             m—m—T—i—i—i—r—r-r
             i—i—i—i—i—n—rr
              i  i  i   i   i  i   i    i
i   i
         0.01 0.060.10.2 0,5  1
                                 10
                                     20  30 40 SO 60 70  SO
                                                           90
                                                                  98 9999.599.899.9
                                                                                  99.99
                PERCENTAGE OF TIME STREAMFLOW, SUSPENDED-SEDIMENT CONCENTRATION,
                   AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED
         Figure 4B.  Long-term daily streamfluw and June 1975-May  1977 mean
                     daily  streamflow, suspended sediment concentration, and
                     suspended sediment discharge,  Genesee River at Portageville.
                                        1-46

-------
  10,000
   1000 -
CJ
UJ
V)
I

g
y
CO

u
100
     10
    0.1
           i  i  I   i   I  r
                                                                i  i
           ill   til
                            1
I   i   i   i  I   i   i
J	I
I   I  I  I  I
                                                     80
                                                         90  95
                                                                 98 9999.599.899.9
      0.01  0.050.10.2  0.5 1   2    6   10  20  30  40 SO 60  70

                  PERCENTAGE OF TIME STREAMFLOW WAS EQUALED OR EXCEEDED


   Figure  4C.   Long-term daily streamflow and  June 1975-May 1977 mean
                daily streamflow, Canaseraga Creek above Dansville.
                                                                                 99.99
                                       1-47

-------
 10.000
   1000 -
Q


o




QC
LU
Q.
y
m

U
    100 -
      0.01  0.050.10.2  0.6 1   2    5   10  2O  30 40 SO 60 70  80   90  96   98 9999.599.899.9   99.99

                  PERCENTAGE OF TIME STREAMFLOW WAS EQUALED OR EXCEEDED



       Figure  4D.   Long-lerm daily streamflow and June  1975-May 1977  mean

                    daily  streamflow, Keshequa Creek at  Sonyea.
                                      1-48

-------
     100,000
     10,000
to
£^§  1000
CL «= LU

g-J
2^  '00
IP
IsS
        10
                                               I  I
              I  i  I  I   i  I   i    i
                      I	LI  i   i
I
         0.01 0.050.10.2 0.5  1  2
   Figure 4E.
                 10  20  30 40 50 60 70  80  90  9S   98  9999.599.899.9
 PERCENTAGE OF TIME STREAMFLOW, SUSPENDED-SEDIMENT CONCENTRATION,
   AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED

Long-term streamflow and June  1975-May 1977 mean daily stream
streamflow,  suspended sediment  concentration and suspended
sediment  discharge, Canaseraga  Creek at Shakers Crossing.
                                                                                  99.99
                                       1-49

-------
    100,000
     10,000
tr —''
rr-. — i
Ufiji
      1000
       100
        10
                     r~n—\—r
T — i   i  i — i — i
 1 — i
                                  i — rr
              iii
i   i   i  i   i  i   i
j
                          i   i  i   i  i
         1
         0.01  0.050.10.2 0.8  1  2   5   10  20  30 40 SO 60 70  80   90  95   90  9999.599.899.9   99.99

                 PERCENTAGE OF TIME STREAMFLOW, SUSPENDED-SEDIMENT CONCENTRATION,

                   AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED

       Figure  4F.   Long-term, daily  streamflow and June  1975-May 1977 mean daily

                    streamflow,  suspended sediment concentration, and suspended

                    sediment discharge,  Genesee River  near Mt.  Morris.
                                       1-50

-------
100,000
 10,000
   100
    10
         TTT—rr~-i—r
    i   i  I   I  i—i—i—i—r—n—r
         i  i i  i  i   i   i    i
A  J  L  I  J  I   I
I
I  I
I
    0.01 0.050.10.2  0.6  1  2   S   tO   20  30 40 SO 60 70  80   90  95   98  99 99.S99.899.9  99.99
            PERCENTAGE OF TIME STREAMFLOW, SUSPENDED-SEDIMENT CONCENTRATION,
              AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED
 Figure 4G.  Long-term daily streamflow and June 1975-May 1977 mean  daily
              streamflow,  suspended sediment concentration,  and suspended
              sediment discharge, Genesee River  at Avon.
                                   1-51

-------
1000
 100
 10
 0.1
0.01
ill  111 — \ — I
                                                      i — i — r— r— i — rr
       i i  i   i  i   i    i   i
                        i
i   i  i
                                              i
i   i
                                                                     i
  0.01 0.050.10.2 0.5 1   2    5   10   20  30 40 SO 60 70 80   90   95   96 9999.599.899.9
               PERCENTAGE OF TIME STREAMFLOWWAS EQUALED OR EXCEEDED
                                                                     99.99
 Figure 4H.   Long-term  daily streamflow and June  1975-May 1977  mean daily
              streamflow,  Oatka Creek at Warsaw.
                                 , 1-52

-------
 10,000
   1000
    100
     10
    0.1
            I I  I  I
           iii   i  i   >
i    i    i  i   i  i   i   i
i   i  i
      0.01 0.050.10.2 O.S 1   2   5   10   20  30 40 SO 60  70  80   00   95   96 99 99.8*9.899.9
             PERCENTAGE OF TIME STREAMFLOW. SUSPENDED-SEDIMENT CONCENTRATION,
                AND SUSPENDED-SEDIMENT DISCHARGE WAS EQUALED OR EXCEEDED

Figure  41.   Long-term daily  streamflow and June  1975-May 1977 mean daily
             streamflow,  suspended sediment concentration and suspended
             sediment discharge,  Oatka Creek at Garbutt.
                                                99.99
                                    1-53

-------
    100,000
     10,000 -
  tr
  LU
  t- >-
    LIJ
O
-------
                       PART II




HYDROGEOLOGIC  INFLUENCES  ON SEDIMENT-TRANSPORT PATTERNS




         IN THE GENESEE RIVER  BASIN,  NEW YORK




                            by




Lawrence J. Mansue, Richard A.  Young,  and Julian Soren




                U.S.  Geological Survey




                Ithaca, New York,  14850
           Prepared in cooperation with  the



New York State Department of Environmental Conservation



               Bureau of Water Research




                Albany, New York, 12233






         U.S. Environmental Protection Agency




                  Chicago, Illinois

-------
                            CONTENTS - PART II

Abstract	•	    i
Figures.	  ii
Tables	  iii
Conversion factors and abbreviations	  iv
Acknowledgments	    v

     1.   Introduction	    1
            Purpose of study	    1
            Scope	    *
            Method	    1
     2.   Summary and conclusions	    3
     3.   Genesee River basin	    5
            Physiography	    -*
            Bedrock and surf icial geology	    8
            Soils	  10
            Land use	  ^
            Channel geology and stream characteristics	  10
            Gradient s	  H
     A.   Sediments	  17
            Suspended sediment	  1?
               Suspended-sediment loads.	  1?
               Seasonal variation	  3.9
               Average annual load and yield.	  20
            Bed material	  20
            Physical properties	  20
               Particle size	  20
               Atterberg limits	  21
            Mineralogy	  25
            Reservoir sampling	  26
     5.   Sediment transport	  27
            Genesee River basin	  27
            Subbasins	  27
               Mill Creek	  27
               Stony Brook	  28
               Genesee River reach from Belmont to Portageville....  28
            Long-term erosion and deposition rates	  28

References	  32

-------
                                  ABSTRACT

     Sediment  loads  transported by streams in the Genesee River basin were
studied from 1975  to 1977  to determine their sources, composition, distri-
bution, movement,  and relation to land use and basin geology.  The basin  is
characterized  by forested  uplands, farmlands in the central part, and urban
development in the vicinity of Rochester at the basin's mouth on Lake Ontario.
However,  the sediment loads and composition seem to be more related to preci-
pitation  patterns  (including snowmelt) and basin geology than to land use.

     Reaches of the  Genesee River's main stem were differentiated by geologic
and channel-gradient conditions.   Sediment loads and composition in the
reaches varied according  to precipitation, runoff, geology, topography,
availability and erodability of sediment-source materials, land use, and  arti-
ficial channel controls.   The sediments were predominantly silt and clay  con-
sisting mostly of  quartz,  plagioclase, illite, and chlorite.

     Major sources of sediment in the Genesee basin are unconsolidated depo-
sits of till on the  uplands,  lacustrine deposits of glacial and Holocene  age,
and deltaic or outwash deposits of glacial origin In valley areas.  The uncon-
solidated deposits are largely derived from underlying bedrock that consists
predominantly  of limestones,  shales,  and siltstones in the lower part of  the
basin and siltstones and  sandstones in the upper part.

     Sediment  loading and  deposition seemed to migrate downstream in a
pulsating manner in  response to precipitation and changing channel gradients
in the Genesee's main stem and in major tributaries during the study.
However,  these streams have mature characteristics, and fluctuating patterns
of sediment load and deposition are normal in the channels of such streams.

     It seems  that not all sediment in the Genesee's main stem is currently
transported out of the basin.   Suspended-sediment load at Portageville, about
halfway down the basin, averaged  1,080,000 megagrams in 1976-1977; Canaseraga
and Oatka Creeks,  tributaries that enter the main stem below Portageville,
contributed an additional  combined average load of 233,000 megagrams to the
main stem in the same years.   At  Rochester, the sediment load in these years
averaged  1,060,000 megagrams.   Thus,  a minimum of 253,000 megagrams seems to
have been deposited  in main-stem  reaches above Rochester in 1976-77.  The
deposition occurred  behind dams and in stream reaches of low gradients.   Most
of the suspended-sediment  load measured at Rochester was probably discharged
into Lake Ontario.
                                     Il-i

-------
                                   FIGURES

Number                                                               Page
         Map showing physical divisions and  boundaries  of  principal
         stratigraphy groups in the Genesee River  basin	

         Map showing data-collection sites in the Genesee  River
         basin.	
                                    PLATE
          (on file at NYSDEC, Albany,  NY and GLNPO,  Chicago, IL)

          Generalized surficial geology  of  the  Genesee  River
          basin, New York
                                    Il-ii

-------
                                  TABLES
Number                                                               Page

  1       Summary of  stratigraphy  and  geologic units in the
          Genesee River  basin	    9

  2       Land use  in  the  Genesee  River basin:
             Genesee River ma ins tern.	   12
             Canaseraga  Creek  subbasin	   12
             Oatka  Creek subbasin.	   13

  3       Description  of Genesee River segments...	   14

  4       Streamflow and sediment  measuring stations at which
          data were collected  during  1975-77..	   18

  5       Drainage  area  and  1975-77 average measured and
          calculated annual  suspended-sediment load and yield
          at stations  sampled  in the  Genesee River basin	   22

  6       Particle-size  distribution  within suspended-sediment
          samples from Genesee River  basin sampling stations,
          1975-77	   23

  7       Atterberg-limits determination on Genesee River basin
          soil samples......	   24

  8       Dates  from carbon-14 analyses, Genesee River basin	   30

-------
            FACTORS FOR CONVERTING INTERNATIONAL SYSTEM (SI)


          UNITS TO INCH-POUND UNITS AND ABBREVIATIONS OF UNITS
Multiply SI unit





millimeter (mm)


meter (m)


kilometer (km)
 Length


  0.0394


  3.281


  0.6215
to obtain inch-pound unit





inch (in)


foot (ft)


mile (mi)
hectare  (ha)


square kilometer  (knr)
   Area


  2.471


  0.3861
acre
               2
square mile  (mi )
 cubic hectometer  (hnr)
                                  Volume
810.7
acre-foot  (acre-ft)
 megagram (Mg)
  Weight


  1.102


  0.9842
 ton [short,  2,000 pounds  (lb)]


 ton (long,  2,240 lb)
 meters per kilometer (m/km)
  Slope


  5.28
 feet per mile (ft/mi)
                                    Il-iv

-------
                              ACKNOWLEDGMENTS

     This study was  part  of  Task C (pilot studies of watersheds and  sub-
watersheds) of the Pollution from Land Use Activities Reference Group
and was funded through  the U.S.  Environmental Protection Agency (EPA)
and the State of  New York.   The  authors acknowledge the guidance, support,
and advice received  from  Drs.  Leo J.  Hetling and G. Anders Carlson of  the
New York State Department of Environmental Conservation, Bureau of Water
Research, and Robert B. Dona,  Project Officer of the U.S. Environmental
Protection Agency.   Dr. E. H.  Muller  of Syracuse University provided
unpublished data  for the  Genesee River basin map (pi. 1), which incorporates
part of his published map (Muller, 1977).
                                     II-v

-------
                                  SECTION  1

                                INTRODUCTION
     Concern over the effects  of  various  land-use activities on water quality
of the Great Lakes led  the  governments  of the United States and Canada, under
the Great Lakes Water Quality  Agreement of April 5,  1972, to direct the Inter-
national Joint Commission (IJC) to  study  the  impact  of land-use activities on
the Great Lakes and  to  recommend  remedial measures for maintaining or
improving the lakes' water  quality.   In response, the IJC established the
International Reference Group  on  Great  Lakes  Pollution from Land-Use
Activities, referred to as  the Pollution  from Land-Use Activities Reference
Group (PLUARG), to carry out such studies.

PURPOSE OF STUDY

     The Genesee River  basin in New York  was  one of  several watersheds
selected by PLUARG for  study by the U.S.  Geological  Survey.  The purpose of
the study was to collect data  on  streamflow,  water chemistry, sediment
transport, land use, soils, and geology.   This report describes the rela-
tionship of the basin's geology to  the  river's sediment-transport patterns.
Other elements of work  done for the PLUARG study are given in companion
reports described in following sections.

SCOPE

     The scope of the study done  by the Geological Survey included collection
of sediment samples  for mineralogic analyses  and correlation of sediment
material with the geology of the  Genesee  River basin.  Data were collected at
32 stations in the Genesee  basin  from October 1975 to September 1977 to define
the composition and  points  of  origin of sediment transported.  Results of  the
streamflow and suspended-sediment analyses are given in Part I of  this volume
 (Mansue and Bauersfeld, 1983).

METHOD

     The stations used  for  hydrologic-  and sediment-data collection from
1975-77 were selected as representative of the principal types of land use
(cropland, pasture,  residential,  and forest)  within the Genesee watershed.
Streamflow and sediment data consisted  of continuous (daily) and instantaneous
(partial) records with  a main  emphasis  on suspended-sediment loads, but
streambed and source materials were also  collected for study.  Suspended-
sediment samples were analyzed for  concentration, particle-size distribution,
and mineral composition.  Concentration data  were used to calculate suspended-
sediment loads.  Particle-size distribution and mineralogic data were used to

                                    II-1

-------
define the nature of  the  sediment  transported and to identify the source
areas.  Interpretation  and  statistical  analyses of the streamflow and
suspended-sediment data are presented  in Part I of this volume (Mansue and
Bauersfeld,  1983).

     Geological investigation  of  the  Genesee basin included compilation and
mapping of the area's Paleozoic bedrock and Pleistocene glacial unconsolidated
surficial deposits to define the  geologic units' areal extent and to determine
the effect of these units on relative  long- and short-term erosion and sedi-
mentation rates.  The long  term is considered to be the entire postglacial
period, about 11,000 years; the short  term is the period of data collection,
October 1975 to September 1977.
                                    II-2

-------
                                  SECTION 2

                           SUMMARY AND CONCLUSIONS
     Sediment-erosion and  deposition patterns in the Genesee River basin are
controlled chiefly by the  composition and location of bedrock and glacial
source materials and by  intensity  and areal distribution of precipitation.
Relatively erosion-resistant  bedrock and dense clayey till seem to have inhi-
bited the rate of channel  downcutting in many places.  The bedrock consists
principally of shale, siltstone,  sandstone, and limestone ranging in age from
Ordovician to Middle Pennsylvanian.   Most till consists of poorly sorted
material with clayey and silty  matrices  and is compact and erosion resistant.
Where stream channels are  in  sorted  glacial sand and gravel or Holocene allu-
vium overlying till or bedrock,  lateral  channel migrations have caused acce-
lerated bank erosion and triggered landslides into channels.  This has
contributed a significant  amount  of  sediment to the river, especially south of
Portageville.

     Generally, the suspended material sampled consisted of 10-25 percent
sand, 45-60 percent silt,  and 20-40  percent clay.  The major mineral consti-
tuents of transported sediment  were  quartz and illite, which were eroded from
glacial drift that was largely  derived from the underlying sedimentary rocks.

     Significant amounts of suspended sediment move erratically downstream in
multiple erosion/deposition events during spring periods of snowmelt, storms,
or both; therefore, serious problems as  to sampling or interpretation could
arise in short-term studies or  in  correlations between widely spaced stations.

     The major sources of  sediment along the Genesee River channel upstream
from Portageville are probably  (1) slumping of saturated postglacial
lacustrine silt, clay, and sand overlying compact till near river level, and
(2) erosion by lateral channel  migration into Holocene bank alluvium.  The
largest known landslide  in the  basin (at the Graham Farm, about 3 km south of
Portageville) has been active for  at least 3,000 years.

     Sediment transported  in  Mill  Creek, in the headwaters area of Canaseraga
Creek subbasin, is derived mostly  from along a central gorge incised in thick
glacial drift.  Oversteepening  and subsequent slumping of the banks occur
where saturated fine-grained  glacial sediments overlie compact and relatively
Impermeable till.  Similar conditions were observed in the channel of Stony
Brook near Dansville.
                                    11-3

-------
     About  11,000 years  ago,  the  lower Canaseraga Valley north of Dansville
was occupied by a lake whose  floor  was slightly more than 10 meters below the
present floodplain  level of Canaseraga Creek.   Assuming that all early
postglacial stream  sediments  were impounded in the basin, a comparison of the
modern and  the early  postglacial  sediment loads can be approximated.  It is
estimated that the  modern river carries more than four times more suspended
sediment each year  than  was deposited annually in the center of the old lake
basin between 8,000 and  11,000 years ago.

     Radiocarbon (C-^) data indicate that erosion rates have not been uniform
during the  last 11,000 years.  Alternating aggradation and downcutting have
occurred in some reaches,  which suggests regional climatic variations as the
most likely cause.  Aggradation is  assumed to  have occurred during intervals
of wetter,  cooler weather, and downcutting was more pronounced during warmer,
dryer periods.  Radiocarbon dating  of organic  material in the sediments indi-
cates that  a period of flood-plain  aggradation began about 400 years ago.

     In this study, no significant  relationship was noted between land use and
sediment-transport  rate, mainly because local  precipitation or runoff patterns
and sediment sources  obscure  any  sediment-load increases that could be attri-
butable solely to land use.
                                    II-4

-------
                                  SECTION 3

                            GENESEE RIVER BASIN
PHYSIOGRAPHY

     The Genesee  River  basin drains 6,394 km2, of which 6,150 km2 is  in
western New York.   The  river begins at an altitude of 610 m in northcentral
Pennsylvania,  12  km south of the New York border, and flows northward  for  235
km through New York to  Rochester on Lake Ontario, at an altitude of 74 m.  The
basin includes part of  Potter County in Pennsylvania and, in New York, most  of
Allegheny and  Livingston  Counties and parts of Wyoming, Ontario, Monroe, and
Genesee Counties.   The  river valley is 167 km long and trends roughly  north-
northwest for  62  km from  Pennsylvania to Caneadea, N.Y.; from Caneadea,  the
valley trend is north-northeast for 105 km to Lake Ontario.  The greater
length of river than valley length is due to considerable meandering  of  the
stream.

     Most of the  basin  lies in the Southern New York Section of the Appa-
lachian Plateaus  and includes the Genesee system from the headwaters  to near
the vicinity of Geneseo,  N.Y.   From Geneseo to Lake Ontario, the basin lies  in
the Eastern Lake  Section  of the Interior Plains.  The physical divisions are
as described by Fenneraan  (1946), and their boundaries are shown in figure  1;
site and stream locations are shown in figure 2.  The topography of the
Southern New York Section is that of a mature glaciated plateau of moderate  to
high relief.   The Eastern Lake Section consists of maturely dissected  and  gla-
ciated cuestas and lowlands of low to moderate relief with moraines,  lakes,
and lacustrine plains.

     Although  the topography of the Genesee basin was extensively modified by
glaciation, the northern  and southern parts differ physiographically.  In  the
southern part,  where the  glacial ice was thinner and the rocks more resistant,
glacial scouring  was less.

     Canaseraga and Oatka Creeks are the major tributaries to the Genesee
River.  Canaseraga Creek  is 68 km long and drains 868 km2; Oatka Creek is  97
km in long and drains 559 km2.  Both of these tributaries are much longer
than their valley lengths because of considerable meandering.  Meandering  of
the smaller tributaries is common; streamflow is fairly straight only  for
relatively short  distances in the streams' headwater areas.
                                    11-5

-------
                        78 30'
                                                78"
43'
42
30
 42
                EXPLANATION

               Pennsylvania!! (Middle and lower)
               and Mississippian (Lower)
                                                                      77° 30'
                                                                LAKE ONTARIO
 Devonian (Upper)

 Devonian (Upper to middle)

 Silurian and Ordovician

• Stratigraphic boundary
 Physical-province boundary
 Province-section boundary
                                         EASTERN LAKE SECTION
     ^-—— — Drainage bou=viary
                                    /     'T.     •-"•"-^L/'y" V"r>   X—   \M "*•—*l  I
                                    4^J-\B-^^  — ^!

        SOUTHERN NEW YORK SECTION /'^..--^ *,„.%.  ^-.'"'•^,l"'",'-'—^.'iv...,T:.";^3
               PENNSYLVANIA

            LOCATION MAP
                  10
                                     KANAWKA SECTION
                           20MILES
              10    2'0 KILOMETERS
                                             NOTE- Names of geologic units within
                                                   the Stratigraphic groupings are
                                                   given in table 1
   Base from U.S. Geological Survey
   NY and PA Stale base maps. 1 500.000. 1974
   Figure 1.—Physical divisions  and  boundaries ot principal  Stratigraphic
                 groups  in  the Genesee River  basin.
                                           11-6

-------
                                                   78°
43
42'
30
42
                 EXPLANATION

     .04227500 Stage and daily sediment
                site and number

    ^04231000 Stage-recording and sediment
                partial-record site and number

    A04230470 Stage and sediment partial-
                record site and number
                                                                           77 30'
                                                                     LAKE ONTARIO
         •3.4
Precipitation-recording site

Radiocarbon dating sample
site and number(s) of sample(s);i y-^y
tip of arrowhead is approximate V
site(s) location
       .._.._ Drainage boundary
                                                        '"fl^j5422"5670 A ^  ,  j
                                                        !860TJ5\p42eS&00>!	v  :
                                                        QRO^.t   ^ i~     ".   -  I  I
               PENNSYLVANIA

             LOCATION MAP
                   10
                             20MILES
               10
                     20KILOMETERS
   Base from U.S. Geological Survey
   NY and PA Slate hnse maps. 1-500.000. 1974
   Figure  2.—Location of  data-collection sites in the  Genesee River basin.
                                              II-7

-------
     Stream valleys exhibit  characteristics  associated with maturity along
most of the Genesee River  and  along  the  larger tributaries.  Flood plains are
generally much wider  than  streams, and meanders or meander scars are visible
over most of the valley widths.   In  the  larger valleys, streams flow mostly in
their own alluvial deposits.   The Genesee River exhibits some classical
youthful-stream characteristics  such as  occupation of the full valley width
and falls and rapids  in its  upper course, mostly between Belmont, and the
Mount Morris dam 20 km north of  Portageville,  and at Rochester near the mouth
at Lake Ontario.  Between  Portageville and the Mount Morris dam, postglacial
segments of the Genesee exhibit  meanders that  are deeply incised in bedrock,
and the river contains three falls whose total drop is 98 m.  Near the
Genesee's mouth within Rochester, the river  flows mainly on bedrock, drops a
distance of 82 m over three  controlled-level ponds, and occupies essentially
the full valley width.  However, the river banks at Rochester are artificially
controlled to a significant  degree.   In  general, youthful-stream charac-
teristics are common  only  where  relatively short streams flow from high upland
areas toward the larger tributaries  and  the  Genesee's main stem.  However,
typical fluvial morphology has been  significantly modified by glacial erosion
and deposition throughout  the  basin.

BEDROCK AND SURFICIAL GEOLOGY

     Bedrock consists of  Paleozoic sedimentary rocks ranging in age from
Ordovician at Lake Ontario to  Middle Pennsylvanian in Pennsylvania (fig.  1).
The rocks strike approximately east-west and dip to the south generally less
than 2 degrees.  Ordovician  to Upper Devonian bedrock in the lower (northern)
part of the basin consists of  shale, siltstone, and limestone.  Upper Devonian
to Middle Pennsylvanian siltstone and sandstone predominate in the upper
(southern) part.  Bedrock  is exposed in  parts of the Genesee'8 main stem  and
in many of the small  tributaries' channels of the upland.  However, the larger
valleys downstream have been glacially widened and deepened and are largely
filled with drift covered  by river alluvium.  Major stratigraphic groups
within  generalized boundaries  are shown  in figure 1; the stratigraphy and the
names of the geologic units  within the groups are summarized in table 1.

     Bedrock was glacially scoured from north to south  during the Pleistocene
Epoch,  and the rocks  are  now covered almost entirely by drift that was  depo-
sited as the glacier  advanced  across and melted from the area.  In general,
dense,  gray, clayey and  silty  lodgement  till overlies bedrock in valley bot-
toms, but the  till  is covered  by glacial-lake sediments, patches of outwash,
and deltaic deposits  in many of the valley areas.  Along much of the main stem
of Genesee River and  in many tributaries, dense, gray,  silty till or varved
clay lies beneath a  thin  layer of alluvium at or very close to  the channel.
The upland drift  typically consists of more stony till, numerous small  kames,
lake sediments, and  outwash deposits of sand and gravel in meltwater channels
and deltas.  Postglacial  erosion has removed some of this  drift  on steep
valley  sides,  and,  in places,  hanging deltas mark  former proglacial  lake  levels.

     The surficial  geology is  depicted in plate 1.  This map is  derived from
a  published map by Muller (1977) and additional unpublished work by Muller
(written commun.,  1978).   In this report, geologic units of similar
                                    11-8

-------
             TABLE 1.  SUMMARY OF STRATIGRAPHY AND GEOLOGIC UNITS IN THE
                       GENESEE RIVER BASIN. NEW YORK AND PENNSYLVANIA

Erathem System

Pennsylvanian



Mississippian





u
M
O Devonian
<
o
w
,j

Series
Middle and Lower
Pennsy Ivanian


Lower
Mississippian


•







Middle and Upper
Devonian

Geologic units
>!
Pottsville Formation



Pocono Formation _,


Conewango Formation
Conneaut Group*
Canadaway Group*
Java Formation
West Falls Formation,

Sonyea Formation
,
Genes ee Formation "^
.

Principal
rock types

Sandstone, con-
^ T . j
r giomeratej ana
shale




Sandstone,
* siltstone,
and shale


Shale, siltstone
and sandstone
•Shale and silt-
stone
         Silurian
         Ordovician
 Middle       (Hamilton Group
Devonian      \0nondaga Limestone
                          	UNCONFORMITY	

                          'Upper Silurian     Salina Group
                          Middle Silurian
                          Lower Silurian
               Lockport Dolomite
               Clinton Group

               Albion Group
               Queens ton Formation
                                                                    Limestone
Shale, limestone,
and dolomite
Dolomite
Shale and lime-
stone
Sandstone and
shale

Sandstone and
shale
* Geologic name used by New York State Geological Survey (Fisher and others, 1961).
                                       II-9

-------
sedimentary character are  grouped;  for example,  sand and gravel with different
genetic origins, such as kames  and  beach sand,  are grouped into a lithologic
unit (differences  in geologic origin of these materials do not significantly
alter how the materials are  eroded  or weathered).

SOILS

     County soils  maps published  by the U.S.  Department of Agriculture, Soil
Conservation Service, provided  information for interpretation of soils of the
upland areas not adjacent  to the  stream channels.   The composition of soils in
the glaciated Genesee River  basin reflects that of the surficial glacial
material and, indirectly,  that  of the underlying bedrock.

LAND USE

     A Land Use and Natural  Resources (LUNR)  inventory was assembled by the
New York State Department  of Environmental Conservation to determine the prin-
cipal type of land use in  each  watershed of the Genesee River basin (Hetling
and others, 1978,  table 3).   The  Genesee River basin, especially south of
Portageville, consists predominantly of forest and cropland.  Within the cen-
tral area, forests decrease  and agricultural  (crop and pasture) lands increase
northward to the vicinity  of Rochester, the major urban area in the Genesee
basin.  The highest percentage  of cropland is in the Oatka Creek subbasin.

     Generally, crop and pasture  areas increase and forest areas decrease as
the basin-drainage area increases.   This trend coincides with reduced stream
gradients near the mouths  of the  tributaries  and in the Eastern Lake Section
and northern part  of the Southern New York Section physical divisions.  Urban
development predominates in  the extreme northern part of the basin, near
Rochester.  The land-use pattern, excepting urbanization, is similar in the
Keshequa Creek subbasin, where  cropland Increases downstream from 17 to 34
percent of the total subbasin area  from Nunda to Sonyea.  On the Genesee main
stem, croplands increase from 32  to 45 percent of the total land area from
Wellsville to Rochester.   Percentage of pasture does not increase sig-
nificantly with drainage area;  the  most significant feature is the decrease in
forest lands downstream throughout  the Genesee basin.  Percentages of land  for
major uses are given in table 2.

CHANNEL GEOLOGY AND STREAM CHARACTERISTICS

     Flow of the Genesee River  is significantly affected by several geologic
and man-made controls.  The  river flows in a bedrock channel for relatively
short distances at Belmont,  Fillmore, and Portageville; between Portageville
and the Mount Morris dam,  the Genesee Is developed mostly in bedrock, and much
of the river's channel through  Rochester is in bedrock.  The bedrock resists
downcutting more than  till or lake  sediments and coincides with changes  in
gradients along specific stream reaches.  The different gradients were  used to
divide the main stem of the  Genesee River into segments for study of indivi-
dual sedimentation and erosion  differences.  In at least four  places south  of
Portageville, the  main river channel is confined by bedrock at the channel
margins, and lateral streambed  migration at these sites is greatly restricted.
                                    11-10

-------
      The  identifiable geologic controls of river flow are  presented  in table
 3, which  describes the basic relationship between gradient  and  channel
 geology.   Geologic interpretations pertaining to sediment  loads in  Sections 4
 and  5 of  this report are based largely on the data in table 3.   Table 3 was
 compiled  to  correlate the river reaches having unique geologic  characteristics
 and  gradients with specific erosion and deposition mechanisms in the reaches.
 Column 4  in  table 3 describes the major surficial deposits  through  which the
 river flows  in each reach and the composition of the modern flood plain;
 column 5  indicates the major aspects of the flood plain and channel  shape that
 differentiate the river sections in terms of sedimentation  patterns; column 6
 describes historic flood-plain features (mainly lateral meandering)  that are
 indicative of the historic bank erosion or channel stability; and column 7
 lists factors that are interpreted to be related to the stability of channels
 during the period that areal maps and photographs have been available for com-
 parative  study.

 GRADIENTS

      The  Genesee  River's main-stem reaches comprise 14 segments (segments A-N
 in table  3)  on the basis of geology and stream-gradient changes.  Rock crops
 out  at many  of the segment ends.  The gradient changes are  related  primarily
 to the geologic units in the physiographic provinces through which  the Genesee
 flows.

      Gradients are steepest in the Southern New York Section, in the Genesee
 valley from  Pennsylvania to Mount Morris, N.Y.  In this 107-km  reach,  the
 average gradient  of the valley is 4 m/km.  Within this reach, however,  the
 valley descends 94 m over three falls from 1.5 to 4.5 km north  of Portage-
 ville.  The  Genesee's steepest valley gradient, which averages  29.5  m/km, is
 in this 3-km section.   South of Portageville are several smaller falls.   As
 the  Southern New  York Section grades toward the Eastern Lake Section between
 Mount Morris and  Geneseo, the Genesee's average valley gradient  declines to
 1.5 m/km.  Within the Eastern Lake Section, from Geneseo to  the  Erie Canal at
 the  south end of  Rochester, the river's gradient is 0.25 m/km.   Water levels
 in the Erie  Canal and through the center of Rochester are controlled by  three
 dams,  built  at the sites of former natural falls,  that pond  water at altitudes
 (from south  to north),  of 156, 147, and 119 m above sea level.   Outflow  from
 the  ponds  is artificially controlled.  From the base of the  third dam,  75 m
 above sea  level,  the Genesee's valley gradient to base level is  0.1  m/km.

      Stream  gradients  in the Genesee's main stem are generally  lower than
 their valley gradients  because of longer stream lengths that result  from mean-
 dering of  the river.   Stream gradients in various segments  of the Genesee are
 given in  table 3.

      The  downcutting of the channel and lateral migration seem  to be reduced
 by the  relatively resistant,  dense, gray till that is present along  much of
 the Genesee  River channel.   Aerial photographs (1938-1976)  show  that lateral
migration  of the  channel (table 3,  column 5) is least where  rock or  relatively
 resistant  till lines  the channel and is greatest in reaches  in  Holocene  allu-
vium  or silty stratified glacial sediments.


                                     11-11

-------
TABLE 2.  LAND USE IN GENESEE RIVER BASIN, NEW YORK
   (Data adapted from Hetling and others, 1978.)
Land
(Upper figure is
Locality

Wellsville
Transit Bridge
Portageville
Mt. Morris
Avon
Rochester
(RG & E)
Cropland

32.3
24,200
28.5
42,580
30.3
77,000
35.3
129,600
39.9
172,300
44.7
284,500
Pasture
Residential
use in watershed area upstream from locality
area percentage; lower figure is land area, in hectares)
Commercial-
industrial
Forest
Genesee River
3.6
2,700
3.6
5,380
4.1
10,420
4.8
17,620
5.1
22,000
4.2
26,700
2.3
1,720
4.0
5,980
3.6
9,140
3.6
13,200
4.2
18,100
6.0
38,200
.3
220
.5
750
.3
760
.8
2,940
.9
3,900
2.6
16,500
49.6
37,150
53.8
80,380
54.9
139,500
47.5
174,300
42.1
181,800
33.8
215,100
Outdoor
recreation
main stem
—
.2
300
.2
510
2.1
7,700
1.9
8,200
1.5
9,550
Wetlands

4.9
3,670
2.4
3,580
2.4
6,100
2.6
9,540
2.6
11,200
4.1
26,100
Inland
water

.3
220
.3
450
.2
510
.3
1,100
.6
2,600
.7
4,450
Miscel-
laneous

6.7
5,020
6.7
10,000
4.0
10,160
3.0
11,000
2.7
11,700
2.4
15,300
Total
area

100.0
74,900
100.0
149,400
100.0
254,100
100.0
367,000
100.0
431,800
100.0
636,400
Canaseraga Creek subbasin
Sugar Creek
Poags Hole
Stony Brook
Mill Creek
Dansville
Rt. 436
Grove land
Bradner
Rt. 36
28.0**
1,390
26.2
6,110
41.5
2,230
44.2
4,110
32.4
12,800
35.1
16,500
49.0
940
3.6
170
4.5
1,050
6.0
320
11.7
1,090
6.7
2,650
7.6
3,560
14.3
280
.5
30
1.0
230
.5
30
5.8
540
2.3
910
2.8
1,310
—
—
.1
20
'—
5.3
490
1.7
670
2.3
1,080
1.0
20
66.9
3,320
64.5
15,030
46.0
2,480
23.6
2,200
51.2
20,300
47.2
22,100
33.7
650
—
.5
120
3.5
190
—
1.2
480
1.1
520
—
.5
30
1.0
230
.5
30
3.6
330
1.5
600
1.3
610
—
.5
30
1.2
280
.5
30
2.2
210
1.3
520
1.1
520
—
—
1.0
230
1.5
80
3.6
330
1.7
670
1.5
700
2.0
40
100.0
4,970
100.0
23,300
100.0
5,390
100.0
9,300
100.0
39,600
100.0
46,900
100.0
1,930
(continued)

-------
                                                TABLE 2.   (continued).
M

»-•
OJ
Locality

Bradner at
Pioneer Rd.
Keshequa-
Nunda
Keshequa-
Tuscarora
Keshequa-
Sonyea
Shakers
Crossing
Mouth of
Canaseraga
Creek

Rock Clen
Warsaw
Pearl Creek
Oatka Creek at
Pearl Creek
Pavilion
Had Creek
Garbutt
Mouth of
Oatka Creek
Cropland

50.6
5,360
17.2
1,450
30.9
4,700
34. 0
6,060
35.6
30,700
35.6
30,800

52.3**
2,140
44.2
4,820
59.5
1,660
45.5
9,510
50.7
14,550
79.3
2,080
55.3
29,200
55.9
31,100
Pasture Residential
Commercial- Outdoor
industrial Forest recreation
Wetlands
Inland
water
Miscel-
laneous
Total
area
Canaseraga Creek subbasin (continued)
8.7
920
9.4
790
9.6
1,460
9.0
1.600
8.4
7,240
8.4
7,260

2.3
90
5.3
580
9.5
270
8.0
1,670
7.8
2,240
.9
20
5.8
2,050
5.7
3,190
.5
50
6.6
550
4.0
610
3.3
590
2.9
2,500
2.9
2,500

.5
20
2.3
250
—
2.2
460
2.1
600
—
1.9
1,000
1.9
1,060
1.3
140
1.3
110
.8
120
.7
130
1.8
1,540
1.8
1,560

—
—
—
.1
30
.9
20
.2
100
.3
170
36.3
3,850
61.3
5,150
52.3
7,950
50.4
8,980
46.6
40.200
46.7
40,300
Oatka Creek
42
1,730
40.8
4.450
31.0
870
38.8
8,110
34.5
9,900
14.2
380
30.8
16,300
30.3
16,800
.8
90
—
.4
60
.3
50
1.0
860
.9
780
subbasin
1.4
150
--
.7
150
.7
200
.9
20
1.0
520
.9
500
.5
50
2.5
210
1.2
180
1.0
180
1.5
1,280
1.5
1,300

2.9
120
6.0
650
—
4.5
940
3.9
1,120
~
4.0
2,110
3.9
2,170
—
1.3
110
.6
90
.5
90
.7
600
.7
600

—
—
—
—
3.8
100
.2
100
.2
110
1.3
140
.4
30
.2
30
.8
140
1.5
1.280
1.5
1,300

—
—
.3
60
.2
60
—
.8
420
.9
500
100.0
10,600
100.0
8,400
100.0
15,200
100.0
17,820
100.0
86,200
100.0
86,400

100.0
4,100
100.0
10,900
100.0
2,820
100.0
20,900
100.0
28,700
100.0
2,620
100.0
52,800
100.0
55,600

-------
TABLE 3.   DESCRIPTION  OF GENESEE  RIVER SEGMENTS

River distance
from mouth
(km)* to down-
Downstream stream bound.! ry
Segment reach of reach
in plate (1) (2)
A Base of
Rochester
Gorge to
mouth at
take Ontario.
B Black Creek
mouth to base
of Rochester
Gorge.



C Honeoye Creek
mouth to
Black Creek
mouth.

0 Conesus Creek
outlet to
Honeoye Creek
mouth.


E York Landing
to Conesus
Creek outlet.




F Route 63
bridge to
York Landing.

G Canaseraga
to Route 63
bridge.





H Mount Morris
to Canaseraga
Creek mouth.
0
Mouth at Lake
Ontario.


13
Base of
Rochester
Corge,



22.5
Black Creek
mouth.


42.6
Honeoye Creek
at mouth.



57.1
Conesus Creek
outlet.




71.8
York Land Ing.

84.1
Rt 63 bridge
(Ledvard
shale forma
base or chan-
nel north of
bridge.


100
Mouth of
Can.isoraga
Average
channel Predominant surflclal deposits
gradient* (glacial and recent)
(3) (4)
Low,
<0.1 m/km.



Low, <0.1
m/km; 3 dam-
controlled
ponds to
south, total
drop In pondi
about 81 m.
Low,
0.02 m/km.



Lou,
0.2 m/km.




Lou,
0.12 m/km.





Low,
01 7 m/lrtn
. I / ID/ Km.

Moderate,
0,28 m/ km
(Alluvial
valley).





Steep,
1.1 m/km.

Obscured by urban development
probably mainly glacial-lake
deposits.


Flood plain mainly alluvium
with shoreline ridges of
glacial lake sands. Flood
plain bordered by lake sands,
silts, and clays.
9

Drum! ins (till) and some lake
clays or silts mantled with
alluvium.


Mainly alluvium with eolian
sand bordering east bank.
Delta and out wash t,inds and
gravels on west sldr of flood-
plain. Flood plain deposits
possibly more Sandy at depth.
Mainly till (large boulders of
Onondaga Limestone) Interbedded
with varved clays. Evidence of
Ice teadvance blocking valley
between York Landing and Conesus
Creek.

Tills and varved clays with


Alluvial silts, sands* some
ve







Fluvial sediments with greater
amount sand and gr.wel particu-
larly thick at Mount Morris
General
channel morphology
(5)
Bedrock or artificial
banks.



Alluvial floodplain
(channel relatively
straight).




Channel sinuous and
constricted by drumltns.
Width from 305 m in north
to 2.4 km in south.

Cut-off meanders Indicate
rapid lateral channel
migration.



Narrow (305 m for 3 km)
and .stable channel may be
a restricting factor in
large floods. Basal chan-
nel scour probably minimal
during high water owing to
resistance of till.
Somewhat wtder than sec-
last 75 years.

Rapid channel shifting
between km 92 and 98.
Stream straight where
against east bank but
meandering in center of
valley.



Rapid channel shifting
1 (HI- 103 km. Lateral
erosion of meanders may
Flood-plain
characterlst ics
(6)
Little incision into
bedrock.



do.






Constricted floodplain
for 10 km. Floodplain
about 1.6 km wide south
of Barge Canal and wider
at mouth of Black Creek.
Flood plain 2.4 km wide.





Narrow flood plain con-
fined in tilt of large
moraine. Little evidence
oT lateral changes.



Narrows to north In section
till and rock threshold at
York Landing.
Flood plain aggregation
able. River overflowed
banks during hurricane
Agnes (1972). Overbank
f landing unconnton due to
Mount Morris dam.


Rapid meander migration
up to 12 m per year.

Bank stability*
Extensively con-
trol led by ma unhide
st rurtures .


Stability probably
high because of
controlled flow.




Till probablv pres-
ent close to surface
at many places.


Low, appears rela-
tively unstable on
basis of meander
migration.


High and generally
stable in till.
Oxbow Lane land-
slide at Km A9
resulting from
saturation of
varves under till.
High, decreasing to
south.

Slab and sliding
easily eroded
alluvial deposits;
low to moderate
gradient; highest
rate of meander
migrat ton where
trees were removed.
Low, coarser depos-
i i *, with steep c li.in-
ncl grjdlf lit s.
     alluvial fan/delta downstream
     from dam.
be a consequent e of d.im
acting .-is sediment t rap
and the slt-t-p >;r.njt*'nt.
                            (ront IniieH)

-------
                                                         TABLE  3.     (continued).

River distance
from mouth
(km)* to down-
Downstream stream boundary
Segment
inflate
I





J






K




L





M












N





reach
(1)
North end of
Gardeau Flat
to Mount
Morris.


South end
to north end
of Gar dean
Flat.



Base of fait
at Portnge-
vllle to
south end of
Gardeau Flat.
Long Beards
Riff to base
of fall at
Portagevllle.


Dam at
Belmnnt to
LOOK Beards
Riff.









Origin to
dan at
Bolmnnt.



of reach
(2)
105
Mount Morris




119
North end of
Cardeau Plat.




129
South end of
Cardeau Flat
(St. Helena).

HO
Base of fall
at Portage-
vllle.


162
Long Beards
Rtff (1 mile
south of
Fill more.








204
Dam at Bel-
mont (rork
beneath dam)
Headwaters
of basin.
Average
channel
gradient*
(3) _
Moderate
to steep.
Average is
0.69 m/km.


Steep,
1.9 m/km.





Steep,
4.7 m/km
with falls
omitted.

Steep,
1.0 m/km.




Strep,
1.5 m/km.











Steep,
2.3 m/km.





Predominant surf trial deposits
(glacial and recent)
<4)
Shale and slltstone
bedrock with sediment
accumul.it ion In Ml, Morris
reservoir.


Tin-filled burled valley
with some bedrock.





Mainly bed rork and falls.




Sandstone and shale at Long
Beards Riff Is exposed across *
entire stream channel and on
both sift PS. Segment has thin
alluvial rover over dense gray
till, bordered bv like sil t s

Thin alluvium over dense gray
till or contorted glacial lake
material. Lacustrine deposits
of both proglaclal Lake Wells-
vtlle (south of Angelica) and
BeUfasi-Fnimore (Belfast to
Portagevi lie) are present along
the valley sides.





Alluvium over glacial deposits
and bedrock.





General
channel morphology
(5)
River Is confined in
a deep valley carved
in bedrock except with
new sediments deposited
behind dam.

Wider and shallower
than downstream reaches
reaches.




Three falls totaling
94 m drop.



River cut off at the
Graham Farm during
Hurricane Agne«; active
lateral migration. CI4
data shows channel has
last 3,400 years.
Many lateral changes
documented by air photos
1938-76. Recent cut off
at Houghton (km 164) and
north of Angelica Creek
mouth (km 187). Channel
may impinge on rock along

Flood-plain
characteristics
(6)
Unstable artificial con-
ditions; intermittent
deposit ion in reservoir.



Silt, sand, gravel, and
some till. Complicated
by periodic flooding and
vegetation clearing after
hurricane Agnes (1972).
Major slumps in glacial
sediment.
Flood plain almost non-
existent.



Flood plain Averages
2.4-3.2 km wide with
adjarcnt relief on the
order of 91 m. Active
lateral migration with

Flood plain relatively
consistent, 1-6 km In
width.






Bank stability*
(7)
Freeze- thaw
effects along
joints and bedding
planes. Slumping
with low stability
of reserve I r silts.
Variable,






Stable from rock
walls.



Low with large
slides in glacial
lake silts. Has
been active for
at least 2,900

Low, in al luvial
sand where till
forms base of
channel. Lateral
hank undercutting
relatively rapid.

valley sides but not gener-
ally constrained by rock.
Depth to rock nay be up
to .several hundred feet
in some places as shown
by well data.
Cuba sandstone may
account for gradient
change near km 217 to
219.







Undetermined.










Undetermined.






* U.S. Army Corps  of HnRlneers, l%7, plates F3-11.
t l.iiw Is less  than or oqn.il in 0.? in/km; moderate K 0.2-1.0 m/km;  hif>h  Is  greater  Ihnn  1.0 m/km (from U.S. Armv Corps of I'm-.lneers, I9h7,
  pl.itos FI9-22).
t ll.ink •it.ihility;  low -  Literal mlp.r.illnn p,ro.irer I linn rh.innel  width,  . h.int>e  h.isml  on mips .mil .lortnl photographs from I9t« in present,
  medium » later.il  mlcr.ltlon eflu.ll to or less than (hnnnol width,  Mgl» = no ihinpe  note.I on m.-jp-..

-------
Lateral migration is most extreme  in  alluvium-filled valleys where rock lines
only the base of the channel,  thus restricting  downward incision.

     From the river mouth to kilometer  100,  streambed alluvium in the channel
consists predominantly of clay,  silt, and  fine  sand, with smaller amounts of
sorted sand- to cobble-sized material.   Upstream and along tributaries, the
alluvium becomes progressively coarser.  Lining of streambed by gravel to
cobble-size material is common in  upstream upland tributaries.
                                     11-16

-------
                                  SECTION 4

                                  SEDIMENTS
     Streamflows were measured, and  suspended  sediment,  streambed material,
and sediment-source material were collected  for  analyses from October 1975 to
September 1977.  Locations of streamflow  and sediment  stations are shown in
figure 2; these and the periods of collection  are  listed in table 4.   Results
of sample analyses  (tables 5, 6, and 7) are  given  in sections that follow.
Detailed studies were made at selected locations to identify and determine the
composition and erodability characteristics  of sediment-source materials.

SUSPENDED SEDIMENT

     Suspended-sediment samples were collected from streams by depth integra-
tion with standardized  equipment.   All samples were analyzed for suspended-
sediment concentration, and  selected samples were analyzed for particle-size
distribution  and mineral  content.   Seven  daily streamflow and sediment sta-
tions  and 26  daily- or  partial-record streamflow and (or) sediment stations
were operated during  the  study  period (table 4).  The sediment data are
available in  releases of  U.S.  Geological  Survey, titled "Water Resources  Data
for  New  York  (volume 1 for water years 1975,  1976,  1977).  Discussion of  these
data and  tabulation of monthly suspended-sediment load  and statistical analy-
sis  are  presented  in Part I  of  this volume(Mansue and Bauersfeld, 1983).

Suspended-Sediment^ Loads

     The  annual suspended~sediment  loads for  the Genesee River at Portageville
during 1976 and 1977 (1,080,000 and 1,090,000 Mg,  respectively)  were  nearly
equal  to those at Rochester (1,060,000 and  1,050,000  Mg).   The  largest  monthly
 loads at Portageville were in February 1976 (666,000  Mg,  62 percent  of  the
 annual total) and  in September 1977 (441,000  Mg,  40 percent of the annual
 total).  The largest monthly loads  for Rochester  occurred also in February
 1976  (468,000 Mg,  44 percent of  the year's  total) and in September 1977
 (437,000 Mg, 42 percent  of  the  year's total).

       Owing to the  local  variation in climate, precipitation, and hydrologic
 conditions,  comparison of the  sediment volumes transported at different  sam-
 pling locations within the  basin must be restricted  to the annual totals; the
 short-term variations are reflected in the range of  the instantaneous and
 daily streamflow  and sediment  records.
                                    11-17

-------
                 TABLE 4.  STREAMFLOW AND SUSTFNDED-SEDIMENT-MEASURING STATIONS AT WHICH DATA WERE  COLLECTED DURING 1975-77
M
M
 I
H*
OO
Period of collection

04221000

04221725

04222300
04223000
04224740
04224775
04224848
04224900
04224930
04224940
04224978
04225000

04225500

04225600
04225670
04225915
04225950
04226000

04227000

04227500
04228370
04228380
04228500
04230320
04230380
04230400
04230410
04230423
04230470
04230500
04231000
04232000
Station number and name*
Genesee River at Wellsville

Genesee River at Transit Bridge
near Angelica
Genesee River near Houghton
Genesee River at Portageville
Sugar Creek near Canaseraga
Canaseraga Creek above Dansville
Stony Brook at Stony Brook State Park
Mill Creek at Patchlnville
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Canaseraga Creek near Dansville

Canaseraga Creek at Groveland

Bradner Creek near Dansville
Bradner Creek near Sonyea
Keshequa Creek at Nunda
Keshequa Creek at Tuscarora
Keshequa Creek at Sonyea

Canaseraga Creek at Shakers Crossing

Genesee River near Mount Morris
Little Conesus Creek near South Lima
Little Conesus Creek near East Avon
Genesee River at Avon
Oatka Creek at Rock Glen
Oatka Creek at Warsaw
Oatka Creek at Pearl Creek
Pearl Creek at Pearl Creek
Oatka Creek near Pavillion Center
Mad Creek near Le Roy
Oatka Creek at Garbutt
Black Creek at Churchville
Genesee River at Rochester
Streamflow
(daily
record)
8/55-9/58,
10/72-9/77
—

—
8/08-9/77
—
8/74-9/77
—
—
—
—
—
7/10-9/35,
7/70-9/76
2/17-3/20
10/55-9/64
—
—
—
—
3/11-9/32,
11/74-9/77,
11/59-9/70,
10/74-9/77
6/03-9/77
—
—
8/55-9/77
—
12/63-9/77
—
—
—
—
10/45-9/77
10/45-9/77
12/19-9/77
Sediment
(daily
record)
4/75-9/77

—

—
4/75-9/77
—
—
—
—
—
—
—
—

—
—
—
~
—
—
—

3/75-9/77

4/75-9/77
—
—
4/75-9/77
—
—
—
—
—
—
3/75-9/77
—
4/75-9/77
Streamflow
(partial
record)
__

2/75-9/77

4/77-9/77
—
2/75-9/77
—
12/74-9/77
7/76-9/77
7/76-9/77
7/76-9/77
12/74-9/77
—

12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
—

—

—
2/75-6/76
2/75-6/76
—
12/74-9/77
—
12/74-9/76
12/74-9/77
12/74-9/77
12/74-9/77
—
—

Sediment
(partial
record)
	

2/75-9/77

4/77-9/77
—
2/75-9/77
12/74-9/77
12/74-9/77
7/76-9/77
7/76-9/77
7/76-9/77
12/74-9/77
12/74-9/76

12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77
12/74-9/77

—

—
2/75-6/76
2/75-6/76
—
12/74-9/77
12/74-9/77
12/74-9/76
12/74-9/77
12/74-9/77
12/74-9/77
—
12/74-6/76

           * Locations shown in figure 2.

-------
     The largest annual  suspended-sediment load was at the Mount Morris sta-
tion, where 1,260,000 Mg—1.75  times  the  1976 annual load—was measured in
1977.  The total streamflow  during  1976 and 1977 was 2,110 and 1,980 hm3,
respectively, the latter of  which was 6 percent smaller than the previous
year's value.

     The sediment load measured at  Avon was similar to that at the Mount
Morris station.  The suspended  load at Avon was 1.4 times greater in 1977 than
in 1976, and  the annual  streamflow  in 1977 was 10 percent less than in 1976.
This seeming  paradox suggests delayed downstream migration of sediment depo-
sited in the  previous year.  However, until more data are available on the
precipitation patterns,  soil moisture, and flow at Mount Morris, this explana-
tion is tentative.  Stream systems  that are well developed generally have ero-
sion and deposition patterns that vary with the volume of water and sediment
load (Lobeck, 1939, p. 165).

Seasonal Variation

     The largest monthly suspended-sediment load transported during 1975-77
was 666,000 Mg at Portageville  in February 1976.  On February 17 alone, 19
percent of the 1976 annual load was transported.  During the late winter
(February-March, the months  of  highest load) of 1976, the sediment yield (load
per unit drainage area)  of the  Genesee River at Portageville was as much as
2.6 times greater than at Rochester.   In  1977, the two highest suspended-
sediment loads were in March and April at Portageville and Rochester, with a
yield ratio of 2:1 for each  of  these  sites.

     Monthly  sediment loads  at  Portageville decreased from February to May
during the study, whereas at the downstream sites, the loads remained high,
which suggest a delayed  downstream  migration of the sediment through the river
system.  Sediment was temporarily stored  in alluvial channel deposits (no
overbank deposits were made  during  1975-77).  Because events such as intense
precipitation or snowmelt can cause several high discharges during a month,
with most such events lasting only  a  few  days, pulsation of sediment-load
deposition (delayed and  intermittent  downstream migration of sediment deposits)
should be expected.  This pulsation of sediment transport may be ehnanced by
temporary channel deposition along  segments having lower gradients.  This
pulsation could give rise to serious  questions in short-term sediment studies
and in comparisons of sediment  loads  at widely spaced stations.  A significant
downstream progression of sediment  takes  place during any major high flow.
For example on September 14, 1978,  the yield at Portageville was 705 times
greater than  that measured at Rochester.   In contrast, the two yields were
nearly equal  on September 15, and,  on September 16, the yield at Portageville
was only 0.3  percent higher. On February 17, 1976, and February 25 and 28,
1977, ratios  of yield at Portageville to  yield at Rochester were high (14:1,
53:1, and 32:1 respectively), all of  which decreased over the next several
days.
                                    11-19

-------
Average Annual Load and Yield

     A method by Miller (1951) was  used to study the amount of sediment
transportd past a  station  during  a  period longer than the actual measurement
period to determine annual suspended-sediment loads and yields.  This tech-
nique makes use of available long-term streamflow data in the form of a daily
mean-value duration curve  and  the mean line of a sediment-transport curve (plot
of instantaneous streamflow and suspended-sediment discharge).  In the tech-
nique, two assumptions are made:  (1)  that the sediment-transport and flow-
duration curves represent  long-term relationships, and (2) that the observed
instantaneous suspended-sediment  discharge has the same relation to the con-
current flow as the mean daily suspended-sediment load and water discharge.
The results are presented  in table  5.   An example of the computations used in
the process is given  in Part I of this volume(Mansue and Bauersfeld, 1983).


BED MATERIAL

     Particle-size and mineralogic  analyses of streambed material from 16
sites in the Genesee  River Basin  are given by Mansue and Bauersfeld (in press,
table 5).  Bed samples in  headwater sites were found to be coarser than those
in downstream reaches but  of the  same  composition as the adjacent local uncon-
solidated materials and rock;  samples  collected farther downstream from head-
water areas have a more homogeneous composition.

PHYSICAL PROPERTIES

     Suspended sediment, streambed  material, and source materials were ana-
lyzed to characterize their physical properties.  Analyses included particle-
size determination on all  types,  as well as Atterberg limits  (defined in a
following section) of source materials.

Particle Size

     The average particle-size distribution of suspended sediment transported
past sampling stations is  presented in table 6.  Generally, the particle sizes
of suspended material transported in most streams in the Genesee basin during
1975-77 consisted  of  10-25 percent  sand, 45-60 percent silt,  and 20-40 percent
clay.

     The percentage of sand transported in suspension by a stream is directly
proportional to stream gradient  and availability of erodable  source material.
For example, suspended sediment  transported by the Genesee River at Wellsville
contained a greater percentage of sand (25 percent) than at Portageville (14
percent); this is  attributed  to  a greater amount of erodable  sandy material  in
the drainage area  upstream from Wellsville and to disturbance of channel depo-
sits by stream improvements and  road construction in the vicinity of
Wellsville.  In contrast,  considerable amounts of predominantly silty  glacial-
lake sediments upstream  from  the Portageville station seem to be the main
source contributing to  the sediment load at Portageville.   The percentage  of
suspended coarse material  transported for significant distances decreases
below Portageville because lesser amounts of  sandy material enter the  lower

                                     11-20

-------
stream gradient  and  also  because a substantial amount is  trapped behind  the
Mount Morris  dam.  The  proportion of sand increases downstream  from  the  dara  as
the river  flows  over an ancient glacial-lake delta below  the dam.  Neither  the
quantity of the  fine sediment retained in the Mount Morris reservoir  nor the
amount of  sand gained from the delta was determined.  The percentage  of  sand
transported by the Genesee River at Avon is less than at  the Mount Morris sta-
tion.  The lower percentage at Avon suggests sand deposition in the  reach bet-
ween the two  sites,  in  which the river flows on till or glacial-lake  clay with
only a thin cover of alluvium for much of the distance.

     The small percentage of sand (table 6) transported by Bradner Creek near
Dansville  (western tributary to Canaseraga Creek, fig. 1) is probably a  result
of the stream's  low  gradient.  The basin upstream from this site consists of
large amounts of sand and gravel overlying dense gray till.  On the  hillsides,
gray silty till  grades  upward into sandy till.  Tributary streams down the
hillsides  probably carry  sand but deposit much of it at lower elevations as
the stream gradients decrease along Bradner Creek.

     Canaseraga  Creek contributes large quantities of clay and  silt  to the
Genesee River's  sediment  load below Mount Morris.  The creek gradient is too
low to carry  many particles significantly larger than silt to its mouth  at  the
Genesee.

     The information in table 6 indicates a downstream decrease in the percen-
tage of sand  transported  by Oatka Creek.  The low percentage measured at
Garbutt station  is probably a result of deposition behind the dam at  Le  Roy
and a low  precipitation intensity during the study period.  The low  percentage
of sand in Mill  Creek at  Perkinsville is attributed to shallow gradients
upstream from the sampling site.

Atterberg Limits

     Soil  shear  strength  is considered a measure of the soil erodability from
areas adjacent to the streams for evaluating the sedimentation patterns  in  the
basin.  Soil  shear strength was estimated by Atterberg-limits analyses (Lynn
H. Irwin,  Cornell University, written commun., 1978).  Atterberg limits  divide
the cohesive  range from solid to liquid state into five stages, or limits,  in
terms of water content.   The test description is presented by Means  and
Parcher (1963, p. 70-83).  The liquid limit less the plastic limit is defined
as the plasticity index,  which is the plastic range of the material  expressed
numerically.  Material  with a high liquid limit and plasticity index  is  more
resistant  to  erosion than material with a low index.

     Unweathered material were collected from eight sites selected to repre-
sent material being  actively eroded.   Analyses of these samples are  given in
table 7.   Samples 1-4 were collected along the Genesee River 3 km south  of
Portageville  at  a site  known locally as the Graham Farm slide, where  the
Genesee River has recently cut off a meander and where the river impinges
against lacustrine and  alluvial terrace deposits on the east side of  the
valley.  Samples 5-8 were collected from the walls of a 30- to 46-m-deep
ravine carved in thick  glacial moraine by Mill Creek in Mill Creek Gorge,  west
                                     11-21

-------
NJ
N)
                 TABLE 5.   DRAINAGE AREA AND 1976-77 AVERAGE MEASURED AND 1975-77 CALCULATED ANNUAL
                           SUSPENDED-SEDIMENT LOADS  AND YIELDS AT STATIONS SAMPLED IN GENESEE RIVER
                           BASIN (from Mansue and Bauersfeld,  1983).






04221000
04223000
04224775
04227000

04227500
04228500
04230380
04230500
04231000
04232000


Station number and name*


Genesee River at Wellsville
Genesee River at Portageville
Canaseraga Creek above Dannsville
Canaseraga Creek at Shakers
Crossing
Genesee River near Mount Morris
Genesee River at Avon
Oatka Creek at Warsaw
Oatka Creek at Garbutt
Black Creek at Churchville
Genesee River at Rochester


Drainage
area
(k»2)
749
2,541
233
862

3,670
4,318
109
528
319
6,364
Measured
average annual
suspended-
sediment load
(metric tons)
44,000
1,080,000
—
222,000

990,000
794,000
—
10,900
—
1,060,000
Calculated
average annual
suspended-
sediment load
(metric tons)
16,900
500,000
21,200
70,200

748,000
601,000
2,160
3,450
925
417,000
Suspended-
sediment
yield
(metric tons
per km^)
23
197
91
81

204
139
20
6.5
2.9
66

       * Locations shown in figure 2.

-------
                           TABLE 6.  PARTICLE-SIZE DISTRIBUTION IN SUSPENDED-SEDIMENT SAMPLES FROM
                                     GENESEE RIVER BASIN SAMPLING STATIONS, 1975-77
M

N>
U)

04221000
04221725
04222300
04223000
04224740
04224775
04224848
04224900
04224930
04224940
04224978
04225000
04225500
04225600
04225670
04225915
04225950
04226000
04227000
04227500
04228370
04228380
04228500
04230320
04230380
04230400
04230410
04230423
04230470
04230500
04231000
04232000
Station number and name *
Genesee River at Wellsville
Genesee River at Transit Bridge near Angelica
Genesee River near Houghton
Genesee River at Portageville
Sugar Creek near Canaseraga
Canaseraga Creek above Dansville
Stony Brook at Stony Brook State Park
Mill Creek at Patchinville
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Canaseraga Creek near Dansville
Canaseraga Creek at Groveland
Bradner Creek near Dansville
Bradner Creek near Sonyea
Keshequa Creek at Nunda
Keshequa Creek at Tuscarora
Keshequa Creek at Sonyea
Canaseraga Creek at Shakers Crossing
' Genesee River near Mount Morris
Little Conesus Creek near South Lima
Little Conesus Creek near East Avon
Genesee River at Avon
Oatka Creek at Rock Glen
Oatka Creek at Warsaw
Oatka Creek at Pearl Creek
Pearl Creek at Pearl Creek
Oatka Creek near Pavillion Center (Pavillion)
Mad Creek near Le Roy
Oatka Creek at Garbutt
Black Creek at Churchville
Genesee River at Rochester
Average
Clay
(<0.004 mm)
26
27
37
32
32
26
27
22
—
22
17
27
22
48
43
38
36
31
44
38
—
—
40
—
28
—
— —
—
—
61
—
25
percentages in sediment
Silt
(0.004-0.062 mm) '(0
50
55
54
54
51
62
59
65
—
46
60
47
56
44
55
51
51
55
43
46
—
—
48
—
50
—
—
—
—
28
—
49
samples
Sand
.062-2.0 mm)
25
18
9
14
17
12
14
13
13
32
23
26
22
8
2
11
13
14
13
16
—
—
12
24
22
9
18
8
16
11
26
16
         *  Locations shown in figure 1.

-------
TABLE 7.  ATTERBERG-LIMITS DETERMINATIONS ON SOIL SAMPLES FROM GENESEE RIVER BASIN

          [Analyses by Cornell University, Department of Agricultural Engineering,
           Ithaca, N.Y.]
Sample number and description
                                             Natural
                                            moisture
                                  Sampling   content   Liquid  Plastic  Plasticity
                                    date    (percent)   limit    limit       index
1.   Graham Farm landslide,        9/16/77     28.5       37       18
    lake material, southern
    end of slump

2.   Graham Farm landslide,        9/16/77     17.1       25       16
    dense, gray till at toe
    of southern end of slump

3.   Graham Farm landslide,          —        13.3      <26^
    sand lens, below lacustrine
    silt and clay

4.   Graham Farm landslide,        9/30/77     21.3       29       14
    dense gray till at cutoff
    and oxbow

5.   Mill Creek Gorge, lake       10/07/77     12.0       14       12
    sediment

6.   Mill Creek Gorge, till at     9/30/77     13.4       19       12
    base of slump

7.   Mill Creek Gorge, at rail-      —        13.3       19       12
    road cut.  Gray till at
    base of slump

8.   Mill Creek Gorge, 30 ft       9/30/77     18.6       20       16
    from surface, brown till
                                                                            19
                                                                        Nonplastic
                                                                            15
 * Refer to text for sampling location.
 t Soil moisture content less than 26 percent cannot be tested, nor could the
   plastic limit be determined.
                                      11-24

-------
of Perkinsville.    Rapid erosion of the moraine in the Mill Creek valley  con-
tributes much  of  the  sediment that is transported by the creek.

      Samples  1 and  4,  from glacial-lake and gray till deposits,  respectively,
had  the highest liquid limits and plasticity indexes, which indicates  that
these  samples  are more resistant to erosion than the others listed  in  table  7.
Samples from Mill Creek's valley had low liquid limits, plastic  limits, and
plasticity  indices  (table 7), which indicates high susceptibility to erosion.

MINERALOGY

      Two-hundred  seventy-four mineralogic analyses were done on  samples of
suspended sediment,  streambed material, and source material.  Results  of  these
analyses are  presented in Part 1 of this volume by Mansue and Bauersfeld
(1983,  table  5);  the  samples described in this section are also  listed in that
report.  The  suspended-sediment samples represent a variety of runoff  con-
ditions.  The  streambed material was collected after a seasonal  high-flow
period, and the source-material samples were collected where material  was
being  rapidly  eroded.

      The samples  represent the major types and ages of glacial material in  the
Genesee River  basin.   Quartz, illite, and chlorite were the major constituents
in the  samples.  Quartz was the major mineral transported at all but the
lowest  streamflows;  this is due to its predominance in the surficial deposits
and  bedrock and its  resistance to weathering.  Most of the drift and lake
deposits in the Genesee basin were derived from the bedrock in the  area.

      The major clay  minerals in the samples were illite and chlorite.   The
predominance  of these  minerals reflects generally insignificant  weathering
since  Pleistocene glaciation.  The ratio of illite to chlorite (mean value
3.39;  standard deviation 1.56) was consistent among all samples, which
suggests a  similarity  from site to site in the materials eroded  from the  drift
and  the underlying  bedrock.  The processes of glaciation seem to have  largely
homogenized the eroded material, although samples from the Canaseraga  Creek
subbasin contained more chlorite than those from the Mill Creek  subbasin.
Chlorite Is more  abundant in the glacial-lake material sampled near Dansville
and  in  sediment transported during low streamflow.

      Comparison of analyses of samples collected during low streamflow on
December 14,  1975,  show similar values for the Genesee River stations  at
Wellsville, near  Angelica, Portageville, Avon, and for the Canaseraga  Creek
station at  Shakers  Crossing (sampled on December 13, 1975); these analyses
suggest that  suspended sediment in the streams at these sites was well
integrated during transport.  Samples from the Genesee River near Mount Morris
differed in that  the quartz and plagioclase values were higher and  the illite
and  chlorite values  lower.  The similarity of values at Wellsville, near
Angelica, Portageville,  Avon, and Shakers Crossing is attributed  to  erosion  of
an ancient glacial lake delta (the Genesee River flowed into the Canaseraga
Valley  subbasin,  which contained a glacial lake).  The variations among the
Mount Morris samples are attributed to influence of the dam upstream from the
site.  A dense gray  till sample (Emo Road south of Patchinville, collected
May  13, 1976)  also differed from the December 14, 1975, samples  in  that the

                                    11-25

-------
latter contained a greater amount  of  quartz  and lesser amounts of illite and
chlorite.  The till generally has  a coarser  granular structure than glacial-
lake material owing to  the lack  of sorting at  the time of deposition.

     Analyses of the variations  in percentages of (1) chlorite within the clay
fraction, (2) plagioclase, and  (3) potassium feldspar in sediment samples from
various collecting locations  showed that  the variability among samples was
generally large enough  to obscure  any significant differences among the sites
represented.

RESERVOIR SAMPLING

     Most sediment deposited  in  a  reservoir  contains a full suite of material
eroded from upstream.   Depth  as  well  as inflow and outflow characteristics of
the reservoir are among the factors that  affect the rate and pattern of sedi-
ment deposition, which  occurs as a stream enters a reservoir.  Samples were
collected from the bottom of  the reservoir on Little Mill Creek (Canaseraga
Creek subbasin, A km east of  Dansville).and  upstream from the Mount Morris
flood-protection dam on the Genesee River.   The material sampled in the Little
Mill Creek reservoir represented sediment deposited since 1938, when the
downstream end of the reservoir  bottom was sealed with marl.  The Mount Morris
reservoir was sampled approximately 1.4 km upstream from the dam.  The
samplings are described in a  written  communication by L. J. Mansue, R. A.
Young, and T. S. Miller (U.S. Geological  Survey, written commun., 1978).
Samples were obtained by coring  to a  depth of 3.5 m.  At a depth of 1.3 m,
fine sediment several centimeters  thick and  of uniform consistency was found;
this material was probably deposited  by runoff during Hurricane Agnes in 1972.

     Selected samples from both reservoirs were analyzed mineralogically
(Mansue and Bauersfeld,  1983,   table 5).    Similar results were obtained,
which suggests that  the mineral  composition  of fine suspended sediments
throughout the Genesee  basin  has been relatively consistent, probably because
of  the relative homogeneity of  the glacial materials and the bedrock from
which they were derived. Larry Smith (New York State University College of
Arts and  Sciences at Geneseo, written commun., 1977, p.  10) obtained similar
results on samples from the Mount  Morris storage reservoir and glacial-lake
sediments near Houghton in  the  southern part of the basin.  Smith's results
suggest  that whether the lake is of  Pleistocene (glacial) or Holocene  (modern)
age, sediments derived  from  lacustrine deposits are similar.  Because  the
sediment  samples were largely homogeneous, detailed mineralogical studies  of
basin sediment would probably not  provide detailed interpretation as to  speci-
fic sediment sources.
                                     11-26

-------
                                   SECTION 5

                              SEDIMENT  TRANSPORT
     Average annual  suspended-sediment loads and yields are presented in table
5; the following  sections  explain  the  sediment-transport patterns in relation
to basin and subbasin  geology.

GENESEE RIVER BASIN

     The suspended-sediment  load at  Portageville was approximately the same as
at Rochester, but  indicates  that not all sediments that entered the lower
Genesee main stem  were transported out of the basin during 1975-77.  Evidence
of deposition is  seen  in  the heed  for  dredging behind the Mount Morris dam and
additional  sediment  deposited in reaches having a low gradient.  The average
load for the 1976-77 water years,  based on contribution of 1,080,000 metric
tons at Portageville and  233,000 metric tons from the Canaseraga and Oatka
tributaries combined compared to the discharge of 1,060,000 metric tons at
Rochester indicates  that  253,000 metric tons remained as deposits in the
Genesee's main  stem.   This residual  load represents a minimum average for the
2 years because sediment  loads from  tributaries and overland sources
downstream  from Oatka  Creek's mouth  were not included in the computation.  The
Genesee River does not have  a significant flood plain from the gaging station
at Rochester to Lake Ontario, and  it is probable that most of the sediment
load at Rochester  is discharged into Lake Ontario.

     Suspended-sediment yield in the Genesee River basin shows a general
decrease as drainage area  is increased, in accordance with sediment-transport
conditions  defined by  Walling (1976, p. 19).

SUBBASINS

     Detailed studies  of  some individual smaller drainage areas in the Genesee
basin were  made to relate  the erosion, sediment-transport rate, and deposition
processes to sediment  source and other factors affecting sedimentation.  These
studies were done  mainly  near Mill Creek and Stony Brook, which are tribu-
taries to Canaseraga Creek,  and the  Genesee River at Portageville; these loca-
les contained large  amounts  of sediment traceable to specific geologic
sources.

Mill Creek

     Mill Creek flows  westward from  Perkinsville into Canaseraga Creek at
Dansville.  The sediment  in  transport  at four sites along the stream was
related to  the geology and ground-water conditions.

                                     11-27

-------
     Slumping caused  by  ground-water seepage along the streambank occurs at
the upper contact  of  dense  gray  basal till with overlying sediments.
Oversteepening of  the  banks by lateral stream erosion and seepage pressure
combine to cause active  bank slumping, which provides some of the sediment.
Most of the sediment  is  contributed where the channel is incised in uncon-
solidated glacial  deposits  that  contain much silt and clay.  Erosion in the
Mill Creek basin has  contributed significantly to the formation of the main
Canaseraga Creek flood plain downstream and to high suspended-sediment yield
measured at the mouth  of Canaseraga Creek.

Stony Brook

     The Stony Brook  subbasin lies  south of Dansville and adjacent to the Mill
Creek subbasin.  Stony Brook enters Canaseraga Creek 1.5 km upstream from
Dansville.  Stony  Brook  has a higher suspended-sediment load per streamflow
unit than was found at other sites  in the Genesee River basin (Mansue and
Bauersfeld,  1983,     table 3).   The geologic setting of the Stony Brook sub-
basin is similar to that of Mill Creek, and it is likely that the erosion pro-
cesses and resulting  suspended-sediment loads in the two subbasins are also
similar.

Genesee River Reach from Belmont to Portageville

     In the upper  (southern) Genesee River basin, the river flows on bedrock
at Belmont, Fillmore,  and Portageville.  Between these localities, dense gray
till occupies most of  the channel.   Vertical downcutting by the river is
retarded by the bedrock  and dense gray till.  The Genesee's main stem south of
Caneadea (table 3, reach M) flows north-northwest, mainly against the west
wall of the valley, and  from Caneadea to Portageville the river flows north-
northwestward, mainly against the east wall of the valley.  In the area south
of Portageville, the  river  parallels bedrock jointing for short distances
(table 3, reaches  L and  M).  A study of bedrock-joint orientation along Rush
Creek near Fillmore (L.  J,  Mansue,  written commun., 1977) suggests a secondary
parallelism of this stream and its  tributaries with the direction of bedrock
joints.  However,  the primary controls for the orientation of the Genesee
River's channel are not  known,  other than that the main valley north of
Caneadea generally parallels the direction of glacial scouring.

     Five locations along the east  side of the river channel between Belmont
and Fillmore  (table 3, reaches L and M) contain areas of major stream-bank
slumping.  Slumping is common also along steeper tributary streams in glacial
sediments.  The largest  slump is on the Genesee's main stem at the Graham
Farm, 3 km south of Portageville, and a large part of the sediment load in  the
Genesee at Portageville  is attributed to lateral erosion of slumped material
by the river  and to runoff from the slumped material into the river.

LONG-TERM EROSION  AND DEPOSITION RATES

     Documentation of historic and prehistoric changes in the stream and
flood-plain surfaces  were sought to define erosion and deposition rates in  the
Genesee River basin.   Dating by radiocarbon analysis of organic materials  in
glacial and stream deposits has  provided data on general erosion and deposition

                                    11-28

-------
rates as far back as  11,000 years  B. P.  (before present).  The geologic ages
and significance of 13  samples  are listed in table 8.  Gross aggradation and
degradation rates on  the  flood  plain have been estimated for areas upstream
from Portageville, near Dansville,  and  downstream from Mount Morris.  The
significance of each  sample is  appropriately explained in table 8; however,
several samples are of  special  significance.  Sample 7 (table 8) indicates
that flood-plain aggradation  in the vicinity of Geneseo began before European
settlers caused an increase in  erosion  by clearing the land.  It is possible
that the burning of forest cover by Indians and increased development of
Indian agriculture could  have started an increase in soil erosion, which
significantly increased sediment loads  in streams.  Although the Indians'
activities are probably a factor that contributed to presettlement aggradation
on the flood plain (Miller, 1973), climatic variation cannot be ruled out as
the primary cause.

     Samples 9 and 10 (table  8) date the transition of the Dansville-Canaseraga
valley from an open lake  to a shallow marshy lake slightly more than 9 meters
below the present flood-plain level at  about 11,000 years B.P.

     Sample 12 (table 8)  indicates that the Genesee River was, at the time of
the sample material's deposition,  close to its present channel bottom upstream
from Portageville more  than 3,300 years B.P. , and sample 13 indicates that the
Graham Farm slide, described  previously, was active at least 2,900 years B.P.
Dating of these samples indicates  that  little channel downcutting has occurred
in the last 3,300 years.
     Radiocarbon  (C)  dating  of  a tree trunk buried by earlier land movements
near the north edge  of  the  Graham Farm slide indicates that slumping had begun
at least 2,900 years  B.P.   (Results of radiocarbon analyses are given  in table
8.)  Dating of an  inplace  tree root found intruding till at river level a
short distance upstream from the  slide suggests that the streambed could not
have been significantly higher (probably no more than 3 m above its present
elevation) 3,000 years  B.P.   A river terrace 18 km upstream from, and  15 m
above the modern  streambed  has a  reported beginning date of 7,590 years B.P.
(Muller and others,  written commun. , 1976, p. 32), which suggests rapid down-
cutting between 7,500 and  3,300 years B.P. but little change since.  Data are
too scanty to permit  a  more detailed correlation of sediment load at
Portageville with  climatologic variations.  Rapid downcutting before about
3,300 B.P. probably  resulted in part from the Genesee River's cutting  toward a
lower base level  before the filling of Lake Ontario and before the subsequent
rise of the Great  Lakes area by elastic rebound after glacial retreat.  It is
also probable that bedrock  and till deposits in the Genesee channel, between
its head and Long  Beards Riff  (river mile 162, table 3), are partly respon-
sible for a slower present  rate of downcutting in upstream reaches.

     The radiocarbon  dating studies have also provided additional confirmation
of major regional  climatic  trends and sediment variations during the past
11,000 years (table  8,  samples 3, 4, 5, 6, 7, and 11).  Downstream from the
Mount Morris dam,  a  correlation of drier climate with downcutting on the flood
plain is indicated when information from the carbon-14 analyses is combined
with pollen studies  in  western New York (Miller, 1973).  Alluvium deposition
has been attributed  to  cooler  wetter intervals (Knox, 1972).

                                     11-29

-------
                                 TABLE 8.    DATES  FROM  CARBON-14 ANALYSES,  GENESEE RIVER BASIN
                                                     [Samples collected by R. A. Young and L. J. Mansue;
                                                      analyses by Teledyne Isotopes, Westwood, N.J.]
Laboratory
sample
no. Location
Age,
years
In
B.P.
Approximate
corrected age,
In calendar
years A.D.
Description of
sample
Significance
                 RAY-GS-1   Geneseo quad.,  meander
                 (I-9822)5  bend  300 m SE of State
                           Highway 20A bridge over
                           Genesee River.  42°46'30"
                           lat,  77"50'30" long.
                 RAY-GS-2
                 (1-9823)
Same as sample 1.
                         410 + 80    1,440 + 90
210 + 80    1,405  + 90
                           Tree  roots  3.9 m below sur-
                           face  of  flood plain at base
                           of  overbank deposits
Log buried on point  bar
5.5 m below flood  plain
                              Shows amount of local
                              deposition and gives
                              age of  last meander
                              migration through area
                                                        Agrees with sample 1
                                                        for migration of last
                                                        point bar through area
M
t-H
 I

O
                RAY-GS-3   Geneseo quad., east     1,450 + 80
                (1-9845)   bank Genesee River,           ~
                           600 m NE of Hemp Pond.
                           77°50'45" lat, 42°47'45"
                           long.
                                       547 + 90
                RAY-GS-4   Same as sample 3.
                (1-9827)
                       1,275 + 80
                                       687 + 90
                RAY-GS-5   Caledonia quad., Lacey  8,140 +  140
                (1-9828)   Road at Dugan Creek
                           Swamp.  42°58'30" lat,
                           77°47'30" long.
                RAY-GS-6   Same as sample 5.
                (1-9829)
                RAY-GS-7   Adjacent to samples
                (1-9830)   1 and 2.
                      11,040 + 160
                                                     470 +  80   1,416 + 90
                           Cored  from log in gravel
                           and  sand 10.6 m below flood
                           plain  surface; 1.5-2.1 m
                           below  present riverbed
                          Log in point bar filling
                          old slough at present low
                          water level, 6.7 m below
                          flood-plain surface


                          Marl at 1.2 m depth below
                          0.9 m of peat on top of
                          1.4 m of peat
                          Peat 2.6 m to 2.7 m depth
                          on gray lacustrine clay at
                          base of bog.   Bottom of
                          1.4 m section of peat below
                          sample 5
                          Charcoal from hearth 1.8 m
                          below flood plain.  Many
                          hearths at or near 1.2 m
                          depth associated with
                          buried soil profile
                              Possible period of slightly
                              greater incision before
                              present.  Alternatively
                              indicates little or no
                              net change during this
                              period (1,400 years)

                              Indicates channel near
                              same elevation at time
                              Indicated with no lateral
                              migration until present
                              to expose log

                              Probably Indicates wetter
                              climate or higher water
                              table.  Date on marl is
                              less reliable.  Probably
                              1,000 to 1,500 years too
                              old (based on other data
                              from same bog).

                              Dates probable postglacial
                              period of climatic wanning;
                              places limit on youngest
                              glacial lake in this part
                              of Genesee Valley
                             Presumed  to record beginning
                             of prehistoric alluviation
                              continuing to present
                                                                    (continued)

-------
                                       TABLE  8  (continued).
Laboratory
sample
no. Location *
Age, In
years B.P.
Approximate
corrected age,
In calendar
years A.D. Description of sample
Significance
RAY-GS-8   Dansville quad.,  Red      <180 BP
(1-9831)   School Road at  Bradner
           Creek.  77°44'52" lat,
           42°37'00" long.
RAY-GS-9   Sonyea quad.,  Pioneer   10,730 + 150
(1-9952)   Road at Erie-Lackawanna
           railroad.  77°49'00"  lat,
           42°41'15" long.
RAY-GS-10  Sonyea quad.,  Erie-      11,160 + 160
(1-9972)   Lackawanna railroad
           at Keshequa Creek.
           77"49'39" lat,
           42°41'50" long.

RAY-GS-11  Same as samples           6»015 ± 12°
(1-10,068) 5 and 6.
                    Log buried 1.8 m below
                    flood-plain surface (now
                    covered by dike).   Much
                    organic debris and logs
                    in gray sand

                    Lake clays with organic
                    debris below conspicuous
                    basal peat layer at 9.3 m.
                    Washed residue from 9.4-
                    10.6 m depth in core

                    Wood and peat layer over-
                    lying lake clay section
                    (as in sample 9).  Dated
                    25-mm diameter wood frag-
                    ment with branches.

                    Compact peat below marl
                    layer dated at 7,125 +
                    140 BP (marl date is
                    obviously too old),  (Refer
                    to sample 5 for comparison)
RAY-GS-12  Portageville quad.,  NE   3,375 +
(1-10,076) of Bluestone near Graham
           Farm cutoff, at  west bank
           of Genesee River.
           42°32I33" lat,  78°03'03"
           long.
RAY-GS-13  Portageville quad.,  NE
(1-10,077) of Bluestone near Graham
           Farm,  east  bank at toe
           of large northern slide.
           42°32'43" lat,  78°02'58"
           long.
                                    2,925
90 1,630 + 120 B.C. Tree-root fragment (black),
                    embedded in till exposed by
                    erosion of hurricane Agnes
                    (1972) at low-water level
                    in side of channel
90 1,095 + 155 B.C. Log 0.6-0.9 m above low
                    water in river bank buried
                    by old movements of slide;
                    in 30-46 cm of brown gravel
                    on till and covered by de-
                    formed varves from slide.
                    Bark covered tree with
                    branching.  Probably rep-
                    resents primary burial by
                    slide not reburial of an
                    older trunk.
                                                  Shows recent marked lateral
                                                  migration and(or)  aggreda-
                                                  tion in Canaseraga Valley
                                                  Marks apparent end of
                                                  open lake and beginning
                                                  of shallow marsh-lake
                                                  environment in Canaseraga
                                                  Valley

                                                  Marks apparent end of
                                                  open lake and beginning
                                                  of shallow marsh-lake
                                                  environment in Canaseraga
                                                  Valley

                                                  Marks probable end of dry
                                                  Interval prior to onset of
                                                  marl formation during higher
                                                  water table condition (for
                                                  marl)

                                                  Marks former low Incision
                                                  of streambed at or near
                                                  present level
                                                  Demonstrates early movement
                                                  of slide; in close agreement
                                                  with river incision of
                                                  sample 12
* Locations shown in  figure  2.
t Correction date from Ralph, Michael,  and  Itau,  1974.
t Quadrangle;  map published  by  U.S. Geological Survey.
'• Tfle
-------
                                 REFERENCES
Fenneman, N. M.,  1946,  Physical divisions of the United States:  U.S.
     Geological  Survey  (map).

Fisher, D. W.,  Isachsen,  Y.  W., Rickard, L. V., Broughton, J. G.,  and
     Offield, T.  W.,  1961,  Geologic map of New York:  New York  State
     Museum and  Science  Service Map and Chart Series, no. 5.

Hetling, L. J.,  Carlson,  G.  A., Bloomfield, J. A., Boulton, P.  W.,  Rafferty,
     M. R., 1978,  Summary pilot watershed report:  Albany, N.Y., New York
     State Department of  Environmental Conservation, Bureau of  Water Re-
     sources, 73 p.

Knox, J. A., 1972,  Valley alluvium in southwestern Wisconsin:   Annals  of
     the Association  of  American Geographers, v. 62, no. 3, p.  401-410.

Lobeck, A. K.,  1939,  Geomorphology:  New York, McGraw-Hill, 731 p.

Mansue, L. J.,  and  Bauersfeld,  W.  R., 1953. Part I: Streamflow  and  sediment
     transport  in the Genesee River basin, New York.  In Volume 4;  Streamflow
     and sediment  transport, Final Report Genesee River Watershed.  USEPA.

Means, R. E., and Parcher,  J. V.,  1963, Physical properties of  soils:
     Columbus,  Ohio,  Merril  Books, Inc., 464 p.

Miller, C. R.,  1951,  Analysis of flow-duration sediment-rating  method  of
     computing  sediment  yield:   U.S.  Bureau of Reclamation, 55  p.

Miller, N. G.,  1973,  Late glacial  and postglacial vegatation change in
     southwestern New York  State:   New York State Museum and Science
     Service Bulletin 420,  102  p.

Muller, E. H.,  1977,  Quaternary geology of New York:  New York  State
     Museum and  Science  Service Map and Chart Series, no. 28.

Ralph, E. K., Michael,  H.  N., and  Han, M. C., 1974, Radiocarbon dates  and
     reality:   Archeology of eastern North America, v. 2, no. 1, p. 1-20.

U.S. Army Corps  of  Engineers, 1967, Genesee River basin—Comprehensive
     study of water and  related land resources:  Buffalo, N.Y.,  v.  IV,
     app. F, 40  p.

          1969,  Genesee  River basin study of water and related  land
     resources:   Buffalo,  N.Y.,  v.  I,  Summary report, 179 p. and additions.

                                    11-32

-------
U.S. Army Corps of Engineers, 1967, Genesee River basin—Comprehensive
     study of water and related land resources:  Buffalo, N.Y., v.  IV,
     app. F, 40 p.

	 1969, Genesee River basin study of water and related land
     resources:  Buffalo, N.Y., v. I, Summary report, 179 p. and additions.

U.S. Geological Survey, Water-resources data for New York, part 1,  surface-
     water records:  Albany, N.Y., U.S. Geological Survey open-file reports
     (released annually since 1964).

Walling, D. E., 1976, Natural and channel erosion of unconsolidated source
     material (Geomorphic Control, Magnitude and Frequency of Transfer
     Mechanisms), in H. Shear and A. E. P. Watson, eds., Workshop on
     fluvial transport of sediment-associated nutrients and contaminants:
     Kitchner, Ontario, International Joint Commission Resources Advisory
     Board Proceedings, p. 1-36.

Wolman, M. G., 1954, A method of sampling coarse river-bed material:
     Transactions of the American Geophysical Union, v. 35, no. 6,
     p. 951-956.
                                   11-33

-------
                           PART III

SOURCES AND MOVEMENT OF SEDIMENT IN THE CANASERAGA CREEK BASIN
                   NEAR DANSVILLE, NEW YORK

                              by

    Lawrence J. Mansue, Richard A. Young,  and Todd S.  Miller
                    U.S. Geological Survey
                    Ithaca, New York 14850
                  Prepared in cooperation with
     New York State Department of Environmental Conservation
                    Bureau of Water Research
                     Albany,  New York 12233
             U.S.  Environmental Protection Agency
                    Chicago, Illinois

-------
                          CONTENTS - PART III
Abstract	       i
Figures	.	      ii
Tables	     iii
Conversion Factors	      iv
Acknowledgments	       v

       1.  Introduction..	       1
             Purpose and scope	       2
             Approach	       2
       2.  Summary and Conclusions	       4
       3.  Canaseraga Creek Basin	       6
             Climate and precipitation	       6
             Land use	       6
       4.  Mill Creek Subbasin..	       9
             Geology	       9
             Ground water	      11
             Geomorphology	      18
       5.  Stony Brook Subbasin	      19
             Geology	      19
             Geomorphology	      19
       6.  Upper Canaseraga Creek Subbasin	      23
             Geology	      23
             Ground water	      24
             Geomorphology	      24
       7.  Canaseraga Creek Flood Plain	      26
             Geology	      26
             Ground water	      27
       8.  Sedimentation	      28
             Data collection	      28
             Suspended-sediment transport in subbasins	      28
             Interstation correlation	      31
             Reservoir sampling	      36
             Physical properties of sediment	      38
               Particle-size distribution	      33
               Atterberg limits	      39
             Mineralogy	      40
       9.  Regional Erosion and Deposition Rates	      45

References	      47

-------
                                 ABSTRACT

     Canaseraga Creek basin was selected as a typical basin of the Genesee
 River system from which to obtain representative measurements of erosion
 and  sediment-transport patterns in the vicinity of the Valley Heads
 Moraine  in western New York.   Its several subbasins exhibit a variety of
 geologic,  hydrologic,  and physiographic conditions that permit correlation
 of erosion rates  and suspended-sediment yields with channel character-
 istics,  surficial and  bedrock geology, ground-water conditions, and
 land-use  practices.

     The  highest suspended-sediment yields are associated with stream-bank
 failure  caused by ground-water movement through stratified glacial deposits
 overlying  lodgment till along deeply incised stream reaches.  Some stream
 reaches  in glacial deposits have a significantly greater depth and width
 than those on bedrock,  which  indicates that rapid erosion of glacial depos-
 its  along  the stream throughout postglacial time has supplied the bulk of
 the  sediment transported from the basin.

     Discharge from the  permeable glacial  sediments contributes directly to
 seepage-related slumping along stream banks in areas of ground-water
 discharge.   Ground-water recharge Is greatest In upstream areas along
 glacially  widened valleys having low stream gradients,  irregular glacially
 formed land  features, and permeable  glacial sediments.

     Sediment erosion and transport patterns within the  several subbasins
 reflect  the  wide  variety of geologic,  hydrologic,  physiographic,  and land-
 use  characteristics.  In contrast to the  upstream areas,  where headwater
 tributaries  in glacial  sediments have  caused accelerated erosion, the
 Genesee-Canaseraga valley flood plain near the mouth of Canaseraga Creek
 has  undergone net  deposition  of 1.2  to 1.8 meters  of overbank sediment in
 the  past 400 years.  This began before settlement  of the region and is prob-
 ably  related to climatic fluctuations  as  well as postsettlement land-use
 practices.

    Carbon-14  dating indicates  that  the modern suspended-sediment load may
 be as much as  four times  greater than  in  postglacial  time,  as evidenced by
 cores from a shallow postglacial lake  that received the combined  flow of
Canaseraga Creek  and the  Genesse River near Mt.  Morris  from 11,000 to 8,000
years ago•
                                      III-l

-------
                                 FIGURES

Number

  1      Map of Canaseraga Creek basin  showing  major  drainage
         boundaries and location of streamflow-,  sediment-,  and
         precipitation-measurment stations	•	
         Map showing surficial geology  of Mill  Creek,  Stony Brook,
         and Canaseraga Creek areas near Dansvilie	       12

         Map showing ice-margin positions of latest  glaciation in
         Mill Creek, Stony Brook, and Canaseraga  Creek areas near
         Dansville	       20

         Graph showing suspended-sediment yield at Mill Creek and
         Stony Brook stations in  relation to yield at  Mill Creek
         station at Dansville, July 1976 to September  1977	       34
                                    Ill-ii

-------
                                 TABLES

Number                                                                 Page

  1      Land use In Mill Creek and Stony Brook subbasins,  1968	     8

  2      Summary of selected borings and well logs	    16

  3      Stations at which streamflow and suspended-sediment
         were measured in the Canaseraga Creek basin, with  dates
         of data collection	    29

  4      Summary of streamflow and suspended sediment in Mill Creek
         and Stony Brook subbasins, 1976-77	    32

  5      Standard error and coefficient of determination of
         correlation of suspended-sediment yield between Mill
         Creek at Dansville and that at Mill Creek stations
         and Stony Brook	    35

  6      Measured suspended-sediment yield and load of Mill Creek
         at Dansville and computed suspended-sediment storm yield
         and load at Mill Creek and Stony Brook stations	    37

  7      Particle-size distribution of suspended sediments obtained
         at Canaseraga Creek basin sampling stations, 1975-77	    38

  8      Atterberg limits for glacial material along Mill Creek
         canyon	    39

  9      Mineralogical analysis of sediment source, streambed,  and
         suspended materials from Canaseraga Creek basin,  1975-77....   41

 10      Dates  from carbon-14 analyses,  Canaseraga Creek basin	   46
                                   Ill-iii

-------
                  CONVERSION FACTORS AND ABBREVIATIONS

    The following factors may be used  to convert  International System (SI)
of metric units to U.S. inch-pound system  units.   These  factors are shown
to four significant figures, but the converted  inch-pound  system equiva-
lents should be consistent with the values for  the SI units.
      Multiply SI units
centimeter (cm)

cubic meter per second  (m-Vs)

kilometer (km)

hectare (ha)

meter (m)

metric ton

square kilometer  (km^)

meter per kilometer (m/km)
   By      To obtain inch-pound units

 0.394     inch (in)

35.31      cubic foot per second  (ft3/s)

  .6214    mile (mi)

 2.471     acre

 3.281     foot (ft)

 1.102     ton (short)

  .3861    square mile  (mi^)

 5.280     foot per mile (ft/mi)
                                   Ill-iv

-------
                                ACKNOWLEDGMENTS

    This study was done  as  part of  Task C (pilot studies of watersheds and
subwatersheds) of the Pollution from Land Use Activities Reference Group of
the International Joint  Commission  and was funded by the U.S. Environmental
Protection Agency (EPA)  and the State of New York.   The authors acknowledge
the guidance, support, and  advice  from Leo J.  Hetling and G. Anders
Carlson of the New York  State  Department of Environmental Conservation,
Bureau of Water Research, and  Robert B. Dona and Ralph G. Christensen of
EPA.
                                   IIl-v

-------
                                   SECTION 1

                                 INTRODUCTION
    Deterioration of  the water  quality  of the Great Lakes has prompted the
United States and Canada to  investigate the effects of various land uses on
waters entering the lake system.   Under the Great Lakes Quality Agreement
of April 15, 1972, the  International  Joint Commission (IJC) was engaged to
study the impact of various  land  uses and to recommend remedial measures
to maintain or improve  the water  quality of the Great Lakes.  Through the
Great Lakes Water Quality Board,  the  IJC established the International
Reference Group on Great Lakes  Pollution from Land Use Activities
(Pollution from Land  Use Activities Reference Group, PLUARG) to make the
studies.

     PLUARG developed a program consisting of four major tasks:

Task A, to collect and  assess management and research information and, in
its later_stages, to  critically analyze the potential implications of
recommendations;

Task B, to prepare a  land-use inventory and an analysis of trends in land-
use patterns and practices;

Task C, to (1) make detailed surveys  of selected watersheds to determine
pollutant sources and their  relative  significance, and (2) assess the
transport of pollutants to boundary waters; and

Task D, to obtain supplementary information on the effects of suspended
materials on the boundary waters, their effect on water quality, and their
future significance under alternative management schemes.

The PLUARG study plan was approved by the Great Lakes Water Quality Board
in March 1974 and by  the IJC in April 1974.

     Task C included  intense investigations of six watersheds in Canada and
the United States that  represent  the  full range of urban and rural land
uses in the Great Lakes basin.   A technical committee and a Task C subgroup
developed and made pilot watershed studies and studied the rates and
transport patterns of selected  pollutants to Lake Ontario, particularly
suspended sediment, phosphorus,  and  chloride.  PLUARG selected the Genesee
River watershed to study surface-water  quality as it is affected by (a)
land use, (b) soils,  and (c) geology  and geomorphology.
                                   III-l

-------
 PURPOSE AND SCOPE

     Because many of the factors designated for study could not be com-
 pletely evaluated in the broader Genesee River basin studies (Mansue
 and Bauerfeld,  1983;   and Mansue, Young, and Soren, 1983)  a represent-
 ative subbasin,  Canaseraga Creek basin, was selected for more detailed
 study of the relationships between erosion, runoff, streamflow, deposition,
 and  sediment transport on a smaller scale.  The Canaseraga Creek basin was
 selected because it contributes a significant amount of sediment to the
 Genesee River.   Its geologic and physiographic characteristics can be extrap-
 olated to other  small basins having similar characteristics.

    The major objectives were to identify the sources of sediment
 transported to the lower Canaseraga basin and to define time and rates of
 sediment transport.   In addition, an attempt was made to compare present-
 day erosion and  deposition rates with presettlement (postglacial) rates.

    Because sediment  samples and streamflow measurements revealed anoma-
 lously large  quantities of suspended sediment during both high and low
 flows,  additional sediment-measurement sites were established in the Mill
 Creek subbasin to (1)  help define the transporting capability of specific
 reaches,  (2)  delineate the sources of sediment,  and (3) identify areas
 yielding abnormally  high or low quantities of sediment.  In addition,  data
 on precipitation and  land use were collected to  assess erosion potential,
 and sediment  samples  were collected for particle-size and mineral analyses.


 APPROACH

    Hydrologic and  sediment data were collected  during 1975-77 at selected
 stations.   In June  1976,  the sites on Mill Creek at Dansville and Stony
 Brook at  Stony Brook  State Park were changed from partial-record
 (sampling  on  random  plus storm basis) to automatic storm-sampling sta-
 tions  wherein equipment was activated when stage rose to a preselected
 level.   The site on Mill Creek near Dansville was an automatic storm-
 sampling  station.  The sites on Mill Creek at Perkinsville and Patchinville
were  partial-record  streamflow and sediment-measurement stations to collect
 sediment-load data  during storm runoff.

    Streamflow and  sediment data consist of Instantaneous and daily values.
 Sediment  data represent mainly suspended sediment but include some bed
material;  sediment  samples were analyzed for concentration, particle-size
distribution, and mineral composition.   The sediment-concentration data
were  used  to  compute  sediment discharge;  the particle-size distribution and
mineral-composition data were used to define the nature of the source
materials  and sediment transported.   Manual depth-integrated suspended-
sediment  samples were  collected by methods outlined by Guy and Norman
 (1970).   Sediment concentration and particle-size analysis were determined
in the U.S. Geological Survey sediment  laboratory in Ithaca,  N.Y.,  with
methods  outlined by Guy (1969).   A calibration coefficient was applied to
the fixed-point  samples  obtained with the automatic equipment through com-
parisons with cross-section sampling.


                                      III-2

-------
    Streamflow and suspended-sediment  discharge  were measured monthly and
also during significant  storms.   The  two  miscellaneous-record sites on
Little Mill Creek were sampled  at random  intervals and during storms to
give additional areal coverage.   Interpretations and statistical analyses
of the Genesee River basin  Streamflow  and suspended-sediment data are pre-
sented in Mansue and Bauersfeld  (1983) and in Mansue, Young, and Soren
(1983).

    Geologic  investigations included  reconnaissance mapping of surficial
deposits, the role of ground water in  erosion processes, and collection of
organic material from glacial and fluvial sediments for radiometrlc age
determinations.  These determinations  were made  on material distributed
thoughout the area in sediments  from  a variety of environments, and from
these determinations, a  partial  chronology was developed for aggradation-
degradation cycles, long-term rates of net sediment deposition, and periods
of significant stream-bank  erosion. The  estimated long-term sedimentation
rates of the  lower Canaseraga valley were compared with sediment loads
measured during 1975-77  in  an attempt  to  discern how recent changes in
land use might have affected the gross equilibrium of the basin.
                                   III-3

-------
                                 SECTION 2

                          SUMMARY AND CONCLUSIONS
    The  Canaseraga  Creek basin consists of six subbasins—Mill Creek, Stony
Brook, upper  Canaseraga  Creek,  Bradner Creek,  Keshequa Creek, and the
Canaseraga  Creek  flood plain north of  Dansville.  This study included all
but the  Bradner and Kt-hequa Creek subbasins.

     More than 40 percent of the  land  in the Mill Creek and Stony Brook
basins is used for  agriculture.   The Mill Creek subbasin contains more
pasture, residential, and commercial land than the Stony Brook subbasin
because  it  includes much of  the  town of Dansville.  Much of the Stony Brook
subbasin, where the terrain  is  more rugged,  is forested or used for
recreation, especially in the vicinity of Stony Brook State Park.

    Most runoff to  streams is from intense summer storms, which produce
significant erosion in the headwaters  areas.  Mill Creek contributes
approximately 11,100 metric  tons  of sediment per year,  and Stony Brook
supplies approximately 4,600 metric tons.  The respective annual yields are
119 and  86 metric tons per km2.

    Most of the calculated 7,850  metric tons of suspended sediment
transported annually past the Mill Creek station near Dansville originates
from stream downcutting  of unconsolidated deposits in the uplands west of
Perkinsville.  The  source material consists  mainly of unconsolidated flu-
violacustrine sediment that  overlies dense gray lodgment till.  Small
slumps and earthflows in the fluviolacustrine  sediments are common where
banks have been oversteepened and undercut along a 3-km reach between
Perkinsville and  Stone Falls.  Because the lodgment till at the base of the
exposed  section is  relatively impermeable, ground water moves along the
till contact, forming hillside  seeps that accelerate slumping, especially
during the spring thaw.   In  addition,  a steep  gradient of 21 m/km through
this same section increases  channel erosion  where the main channel has
eroded through the  Valley Heads Moraine.

    The Mill Creek  main  stem was  divided for this study into four sections:
headwaters to Patchinville,  Patchinville to  Perkinsville, Perkinsville to
Stone Falls, and  Stone Falls to Dansville.  Above Patchinville, exposed
bedrock and steep gradients  contribute to rapid runoff and high sediment
discharge per unit  drainage  area  despite thick sand and gravel deposits
that are relatively permeable.  The broad valley near Wayland is underlain
by marl beds, peat, lacustrine clay, and glacial outwash in the low-
gradient segment  from Patchinville to  Perkinsville; the low relief and
impermeable sediments create wetland areas where downward percolation of


                                     III-4

-------
 ground  water is inhibited by the underlying marl, fine-grained glacial-lake
 deposits,  and till.   Low stream velocities and low suspended-sediment
 measurements in this area reflect the low gradient.

     From Perkinsville to Stone Falls, the gradient is steep  (28 m/km).   For
 3  of the 5 km,  the stream has formed a steep ravine by incising as much  as
 30 m into  the Valley Heads Wbraine.   The stream is now cutting into a com-
 pact lodgment till above which are silty fluviolacustrine sediments
 that are involved in most of the stream-bank failures.  From Stone Falls  to
 Dansville,  the  streambed has a conspicuous armor of cobbles  resting on the
 dense gray till;  this armor is slowing the cutting action of the stream.

     The Little  Mill  Creek tributary contributes relatively low con-
 centrations of  suspended sediment.  This basin is covered by permeable
 sandy till and  patches of sand and gravel and also contains a small storage
 reservoir.   Downstream from the reservoir,  the channel is incised in
 bedrock to  its  confluence with Mill Creek.

     The physiographic and geologic setting of the Stony Brook subbasin is
 similar to  that of Mill Creek and thus has  a similar sediment-transport
 regime.  In the uplands,  most of the tributaries are eroding into till and
 outwash and contain  little or no alluvium.   The upper Canaseraga Creek sub-
 basin also  is similar to the Stony Brook subbasin in its sediment-transport
 regime.

     The Canaseraga Creek flood plain below Dansville has undergone deposi-
 tion since  postglacial time,  in contrast to the upstream basins, which have
undergone  erosion.   Radiometric age  determinations on wood samples from
peat  resting  on glacial-lake sediments beneath the Canaseraga flood plain
indicate that the  depositional surface 11,000 years ago was approximately
9 m  below  its present  level.   Data on suspended-sediment discharge farther
downstream  indicate  that  modern erosion rates in the Genesee River basin
may  be  four  times  greater than 8,000 to 11,000 years ago,  when the sedi-
ments of the  former  lake  bottom were deposited.

    Carbon-14 analyses  of wood samples from elsewhere in the Canaseraga
flood plain verify that  stream-channel migration has become extremely
active  over at  least  the  last 180 years.
                                    III-5

-------
                                SECTION  3

                         CANASERAGA  CREEK BASIN
CLIMATE AND PRECIPITATION

    The climate of  the basin  (fig.  1)  is  humid  continental and is charac-
terized by cold, dry winters  and warm,  wet  summers.   The most common storms
are frontal cyclones, which are most frequent from  October to March, and
air-mass storms, which are most frequent  from April  to September (Dethier,
1966, p. 3).  Summer storms account  for more than half the annual precipi-
tation (Dethier, 1966, p. 6).  The  basin  is within  the Western Plateau and
Central Lakes climatological  divisions  and  lies within a rain shadow caused
by orographic precipitation in the  adjacent highlands to the west (Dethier,
966, p. 10).

    Precipitation data used in this  study are from  National Weather Service
records collected at Dansville and  from U.S. Geological Survey records
collected near Arkport, approximately  5 km  south of  the headwaters of the
basin.  The average annual precipitation  at Dansville from 1917-72 was 86.5
cm; the greatest precipitation intensity  recorded during the study was
3.6 cm/h at Arkport on July 7, 1976.
LAND USE

    Major land uses in  the Mill  Creek  and  Stony Brook subbaslns in 1968 are
summarized in table 1 in  terms of  area and percentage of basin.  The most
significant differences between  land-use patterns  of the two subbasins are
(1) percentage of pasture land,  which  is twice as  high in the Mill Creek
subbasin; (2) percentage  of  residential area,  which is approximately 11
times greater in the Mill Creek  subbasin;  (3)  percentage of commercial-
industrial area, which  is 5.3 percent  in the Mill  Creek subbasin and zero
in the Stony Brook subbasin;  (4) percentage of forest land, which is twice
as great in the Stony Brook  subbasin;  (5)  percentage of outdoor recreation
area, which is zero in Mill  Creek  subbasin and 3.5 percent in Stony Brook
subbasin (which contains  a State park); and  (6) percentage of wetlands,
which is approximately  7  times greater in  the  Mill Creek subbasin.

    The larger percentage of  farmland  (cropland and pasture), residential
area, and commercial-industrial  area  in the Mill Creek subbasin is directly
related to the lower relief.  In both  basins,  the  percentage of cropland
decreases with increasing forest cover in  the  rugged terrain of the
uplands.
                                     III-6

-------
78° 00'
                                                                      EXPLANATION
   Genesee River
       basin
                                       Miscellaneous-record stage and suspended-sediment station
                                       Recording stage and daily suspended-sediment station
                                       Recording stage and partial-record suspended-sediment star
                                       Partial record stage and suspended-sediment station
                                       Recording precipitation station
                                       Radiocarbon site and number
                                       Drainage divide
             Canaseraga
             peek basin
      LOCATION MAP
                                                                   Sugar Creek near Canaseraga
                                                                   Canaseraga Creek above DansviHe
                                                                   Stony Brook at Stony Brook Slate Park
                                                                   Mid Creek at Patchmvilte
                                                                   Miff Creek at Perkmsv
                                                                       Creek near Oansvdte
                                                                   Mill Creek n Dansville
                                                                   Canaseraga Creek near DansviHe
                                                                   Canaseraga Creek at Grove I and
                                                                   Bradner Creek near Dan&viHe
                                                                   Bradner Creek near Sonyea
                                                                   Keshequa Creek ai Nunda
                                                                   Keshequa Creek at Tuscarora
                                                                   Keshequa Creek at Sonyea
                                                                   Canaseraga Creek at Shakers Crossing
                                                                   Genesee River near Mount Morns
                                                                   Reservoir on Little Mill C'eek
 Base from U.S. Geological Survey
  'mira. NY,PA, 1968, 1 ZSO.OOQscale
  Figure 1.-
-Major drainage  boundaries  of  Canaseraga Creek basin  and  location
 of streamflow-,  sediment-,  and  precipitation-measurement  stations.
 (Station numbers and  sampling dates  are given in  table  3.)
                                                  III-7

-------
TABLE 1.  LAND USE IN MILL CREEK  AND  STONY BROOK SUBBASINS, 1968

             (Data from Hetling and others,  1978;
                 area values  are  in hectares)

Land Use
Cropland
Pasture
Residential
Commercial-
industrial
Forest
Outdoor
recreation
Wetlands
Inland water
Miscellaneous
Total
Mill
Percentage
44.2
11.7
5.8
5.3
23.6
—
3.6
2.2
3.6
100.0
Creek
Area
4110
1090
540
490
2200
—
330
210
330
9300
Stony
Percentage
41.5
6.0
.5
—
46.0
3.5
.5
.5
1.5
100.0
Brook
Area
2230
320
30
—
2480
190
30
30
80
5390

                               III-8

-------
                                 SECTION 4

                            MILL  CREEK SUBBASIN


    Mill Creek has  a  drainage  area of 93 km^ and flows west into Canaseraga
Creek, a major tributary  to the  Genesee River (fig. 1).  The main stem of
Mill Creek and its  tributaries have 130 km of definable channel.  The head-
waters of the creek begin 9.6  km southeast of Perkinsville (altitude 648 m).
The main tributaries  flow north  from the uplands into a glacially broadened
east-west valley.   Near the center of the valley floor the channels have
been straightened artifically; two segments parallel the abandoned
Delaware-Lackawanna Railroad for 3 km.  North of the railroad embankment,
wetlands and abandoned marl pits cover much of the valley floor.  The main
tributaries join near Perkinsville, where a deep ravine has been cut
through the main crest of the  Valley Heads Moraine for 3 km to Stone Falls.
Bedrock crops out discontinuously from near Stone Falls to the town of
Dansville.  Along this segment,  Mill Creek is joined by Little Mill Creek.


GEOLOGY

     The Mill Creek subbasin contains glacial deposits associated with the
Valley Heads Moraine(s) of late  Wisconsinan age.  The underlying bedrock
consists mainly of  siltstone and shale of the West Falls group and
generally crops out only  along the lower reaches of major tributaries and
along small gullies on steep upland slopes.

    The main channel  of Mill Creek occupies part of the prominent east-west
glacial trough running from Dansville through Wayland and east.

    A reconnaissance  map  of the  major glacial moraines was drawn by G. C.
Connally (New York  State  Geological Survey, written commun., 1961).
Fairchild (1928) described the surficial geology and postulated events
during deglaciation of the Dansville region, with emphasis on the geologic
formations exposed  near Stony  Brook south of Dansville (fig. 1).

    Remapping during  the  present study suggests that several ideas pre-
sented in these earlier works  require modification.  Unpublished works by
E. H.  Muller, of Syracuse University, and R. A. Young, of the State
University College  at Geneseo, as well as radiocarbon dates obtained during
this study, have added significant information relating to the late
Pleistocene and Holocene  geology.
                                    III-9

-------
    The surficial geology  of  the Mill  Creek subbasin is illustrated in
figure 2.  The highlands are  covered by  relatively thin deposits of stony
to sandy till with patches  of  outwash, generally in the form of kame terra-
ces.  These deposits contrast  markedly with the thicker,  more clay-rich
basal tills produced by multiple advances  or readvances of ice over shale
bedrock and lacustrine deposits in  the main valleys.  Each glacial advance
apparently eroded the highlands but overrode and reworked the thicker gla-
cial-lake silt, clay, and  outwash in the valleys to form new deposits.

    Well logs obtained thoughout the study area (table 2) indicate that
glacial sediments vary considerably from place to place.   They are more
than 137 m thick near Dansville and are  estimated to be as much as 100 m
thick in the valley near Wayland.

    The most conspicuous part  of the Valley Heads Moraine fills most of the
valley between Perkinsville and Dansville.   The morphology and internal
stratigraphy of the moraine along the  main stem of Mill Creek indicates
that this massive moraine was  formed during one or more readvances of ice.
The last major readvance deposited  sandy to gravelly till containing masses
of lacustrine silt and contorted varved  sediments.  This  moraine, formed by
a readvance over lacustrine and deltaic  deposits at the margin of an older
proglacial lake, is a morphostratigraphic  unit of hydrologic significance
to the Mill Creek subbasin  because  it  strongly influences both surface
infiltration and ground-water  movement.   Although the moraines between
Perkinsville and Dansville  are the most  prominent glacial features, the
crests of older moraines and  the trends  of ice-margin outwash channels are
also evident to the south  and  east.  (See  fig. 3.)

    The repeated advances  of  the ice front in this region have been the
principal force in shaping  the morphology  and glacial stratigraphy, and
thus the hydrologic properties, of  the surficial sediments.

    All moraines exposed in stream  banks of Mill Creek basin are composed
of sandy till underlain by  a  clay-rich gray basal till that underlies the
valley floors.  This basal  till, deposited before the Valley Heads read-
vance, resulted from deep  erosion of the shale bedrock north of Dansville
by a massive ice sheet capable of scouring to bedrock.

    Between the basal till  and the  sandy till of the surficial moraines are
deposits of massive gray silt  that  lack  obvious stratification.  This silt
is well exposed in the 46  m of surficial sediments along Mill Creek wsst of
Perkinsville.  The deposits seem to have gradational contacts with the
underlying and overlying tills and  contain scattered lenses of sand and
gravel.  They are interpreted  to be  lacustrine deposits that were over-
ridden and reworked by the  Valley Heads  readvance.  However, any explana-
tion of their precise origin  must reconcile their fine grain size with
their lack of obvious internal structure or stratification.
                                     111-10

-------
     The massive silt and overlying sandy till deposits are,  in  places,
 covered by discontinuous patches of more recent fluvial and  deltaic  sedi-
 ments  from the initiation of the modern drainage as the ice  withdrew  for
 the  last time.  Below an altitude of 305 m, the discontinuous sand and
 gravel beds give way to more uniformly deposited deltaic sand,  which  marks
 the  prominent "1000-ft" (305-m) lake shore that correlates with the Pearl
 Creek  outlet west of Geneseo (Mansue, Young, and Soren, 1983 -  fig.l).

     The veneer of stream gravel and deltaic sand at high elevations  is
 generally oxidized,  and slumping of exposures obscures the contacts with
 the  older deposits.   The zone of oxidation is irregular and  highly variable
 in stream-gully exposures; also it does not seem to conform  to  strati-
 graphic horizons, which further complicates recognition of geologic  rela-
 tionships.
GROUND  WATER

     Despite  the  lack of distinct stratigraphic contacts along the Mill
Creek channel,  the  geohydrologic conditions that affect present-day sedi-
ment erosion are easily recognizable.   The surficial sandy morainic,
deltaic,  and fluvial deposits are highly permeable, as indicated by the
lack of surficial ponding of water in closed depressions in the deposits
between Dansvilie and Perkinsville.   In contrast, the massive water-
saturated silt  beneath these deposits  is subject to slump failure,
quicksand conditions, liquefaction,  mud flows, and general instability
because the-relatively impermeable basal till beneath the silt limits down-
ward percolation of ground water and causes springs and seeps at the upper
contact of  the  till.

     A slightly  different sequence of geologic units east of Perkinsville
has  formed a more complicated geohydrologic regime.  When the ice front was
near Perkinsville (fig. 2), the area near Wayland was a shallow lake,
blocked by ice  on the east and west, in which a deposit of clay formed.
Coarse  outwash  sand and gravel now overlies and interfingers with the lake
sediments around the margins of the  basin.   Well logs taken immediately
south of  Wayland record permeable sand and gravel to depths of 15 to 18 m,
underlain by relatively impermeable  clay.  The area near Wayland is covered
by wetlands,  muckland,  and outwash deposits overlying the less permeable
lake sediments.   Runoff from the adjacent hills enters the permeable sand,
gravel,  and  morainic materials in the  vicinity of Perkinsville and Wayland
and  resurfaces as seepage near the top of bedrock along the Mill Creek
channel above Stone Falls.   This is  inferred to be the major pathway for
ground  water in  the Mill Creek subbasin.

    The distribution of bedrock outcrops  (fig. 2) near Stone Falls suggests
that the  bedrock surface beneath the buried glaciated valley is near an
altitude  of  300  m.   Assuming a moderate westward bedrock slope resulting
from ice  erosion between Wayland and Dansville,  thickness of the drift prob-
ably reaches  90  to  110  m beneath the upper part of the Mill Creek sub-
basin.   No wells  or  exposures  confirm  this  estimate,  however.
                                     111-11

-------
                                                                 77 37'30"
     *
   from U.S. Geological Survey
'W mi nut* QuBorttnglvt, 1978
Figure 2.   Surficial  geology  of Canaseraga Creek, Stony Brook,



                             111-12

-------
                                                 Geology by R.A. Young. 1977
and Mill  Creek  Near Dansville.
                                     111-13

-------
                             FIGURE 2 - EXPLANATION

|w  [ Open-water  areas,  natural  and man-made ponds

[a  j Alluvium:   clay,  sand,  and gravel

     Interpretation:   Modern stream deposits,  maximum thickness approximately
        11 m in  lower  Canaseraga Valley near Mt.  Morris.   Overlying outwash and
        lacustrine  deposits  near Wayland.   A few  deposits in small gullies and
        tributaries are omitted  from map

|pm| Peat,  marl, muck,  and  clay

     Interpretation:   Postglacial  to recent deposits in Wayland area in
        poorly drained  depressions.   Fine  sediments cannot always be
        distinguished  from lacustrine deposits  of late glacial age where
        outcrops  are scarce

     Stratified  sandy  deposits  of  linear  form  at uniform elevations along
        valley sides.   Includes  silts and  gravel

     Interpretation:   Remnants  of  shorelines of  proglacial lake stages during
        final retreat  of  ice  from Valley Heads  Moraine.   Interfingers with delta
        sands (sd)  near  larger streams


Isd | Stratified  sandy  deposits  along major tributary gullies.  Includes silt
        and  gravel

     Interpretation:  Deltaic deposits  associated with  changing proglacial lake
        shorelines.  Gradational  with (si)

     Massive lake  silt,  generally  gray.   Locally includes significant clay,
       gravel, or  ice-rafted pebbles.   Stratification generally not apparent

     Interpretation:  Sorting,  poor  stratification,  and  field relationships
        Indicate  that this material was  deposited in  small,  disconnected pro-
       glacial lakes near ice margin.   Cold-water density currents near ice
        front may have prevented  formation  of distinct varves.   Gradational with
        till below  (tg) and fluvial deposits  above (sd).   May  be largely reworked
       silts from  readvance of  ice over well-sorted  lacustrine deposits in
       Canaseraga  valley with some addition  of sediment  from  tributaries
       draining adjacent upland  areas.  These  silts  are  largely rock flour,  rich
       In quartz,  and seem to be involved  in most of the  active landslides and
       slumps in the Valley Heads Moraine  deposits.   The  silts can easily be
       mistaken for clays when wet and become highly unstable when saturated

[o  | Gravel, sand,  silt, and clay  in well-defined ice-marginal channels

     Interpretation:  Deposits are in channels from  streams near the ice margin
       that are still visible on aerial photos as channelized depressions with
       some braided bed forms.   Closely related  to kame-terrace and outwash
       deposits

|v | Uniformly varved clays and  silts, reddish brown

                                       III-U

-------
      Interpretation:   These deposits are widespread at elevations below 427 m
       and  represent  deposits of the larger proglacial lakes  that formed as the
       ice  retreated  up the Canaseraga-Genesee valley.  Only  large outcrops are
       indicated*   Small outcrops occur in other areas, but in many places the
       soil profile or human activities have destroyed most of the original
       texture.   Contorted remnants of similar deposits are also included  in
       the  tills  of the Valley Heads Moraine (km) as a result of their incor-
       poration  by ice readvancing down the valley to form the moraine.  Most
       exposures  of varves at land surface are younger than the moraine

 jkt |  Stratified  kame-terrace sands, silts, and gravels

      Interpretation:   High-level ice-marginal deposits requiring the presence
       of ice  to  contain the flow along one side of the former channels.
       Locally gradational with (sd) and (km)

 [km j  Sandy  tills  characteristic of the Valley Heads Moraine.  Includes
       sand, silt,  gravel,  and some varved sediments slightly reworked or
       deposited  penecontemporaneously with the moraine

      Interpretation:   The main moraine south of Dansville is characterized by
       kame and kettle topography with a few kettle lakes.  The tills here are
       very sandy  and permeable because of deltaic deposits that were reworked
       by readvance of the  ice down the Canaseraga Valley.  Only such a
       retreat-and-readvance sequence  would explain the sandy nature of the
       moraine, in  contrast to the basal and upland tills

      Gray silty to  clay tills with a few large  clasts

      Interpretation:   This  basal till  at the lower end of the Canaseraga Valley
       was  probably formed  through the reworking of varves deposited in
       proglacial  lakes in  the Canaseraga valley as the ice advanced before the
       Valley  Heads event.   The lack of clasts  contrasts strongly with the
       tills along  the valley sides and on the  uplands.   The gray color is
       attributed both to the position of the till below the water table and to
       its  low permeability.   The content of larger clasts is variable but
       generally low.   This till is exposed at  the base of many slumps along
       tributary streams  but is not as readily  eroded as the lacustrine silts
       (Is) above it

}ts| Brownish  sandy tills of  upland regions

     Interpretation:   These tills  were  deposited at various elevations above
       the main valleys where sandstones and siltstones are close to the sur-
       face.   They  are  more permeable  than the  gray valley till (tg) and vary
       somewhat in  their  content of larger clasts,  thus reflecting local bed-
       rock variations.   The  till  is  in most cases less than 1.5 m thick,  and
       bedrock is exposed in  most  small gullies.  Good exposures are  rare except
       in gravel pits.  Plowed  fields  Indicate  the high pebble and cobble  con-
       tent.   The sandy nature  of  these tills allows  easy percolation of preci-
       pitation in  upland areas  and probably reduces  the  sediment load in  head-
       ward tributaries,  as  compared to the more  clay-rich tills

|t | Till not  readily  related  to (km),  (tg),  or  (ts)

|r | Bedrock exposures. Small  outcrops  in  upland  areas  not mapped

                                       111-15

-------
           TABLE 2.  SUMMARY OF SELECTED BORINGS AND WELL LOGS

Land-surface
elevation
Boring* (meters)
13A 315.8


24A 332.5
33A 364.8
42A 381.0


133D 213
134D do.
142E 324.9


DAF55 174

Well Log2
Perkins ville 1 414.5



Depth
(meters)
Material
Brown silt, sand, gravel
Brown sand
Brown silt (trace sand, gravel,
clay)
Brown to gray silt, trace clay
and sand (till)
Fine to medium gray sand, silt
Brown silt and fine sand
trace clay, gravel (till)
Gray silty sand, trace
gravel (till)
Sand, gravel, clay silt,
trace sand, clay
do.
Sand, gravel
Gray silt, sand, gravel (till)
Rock at
Peat, clay, silt
Gray silt, clay
Gray sandy clay
Gravel
Soft gray clay
Gravel and sand
from
0
6.1
10.1
0
0

0
19.5
1.5
do.
0
3.0
14.9
0
9.8
0
10.1
12.8
14.3
to
6.1
10.1
24.4
15.8
17.4

19.5
21.9
12.5
do.
3.0
14.9
—
9.8
76.2
10.2
12.8
14.3
21.9
1  From New York State Department of Transportation
   (written commun., 1977)
2  From Kammerer and Hobba, 1967, table A-l, A-2.
                                    111-16

-------
TABLE 2  (continued).

Land-surface
elevation
Well Log2 (meters) Material
Perkinsville 2 414.5



Wayland 416.1
(composite of
several wells
in area)
235-743-1 181
234-743-2 189



Composite of 207
borings 3A,
121C, 122C
and well logs
232-741-1
233-742-1, 3


Hard blue clay, gravel (till)
Gravel and sand (outwash)
Gray clay
Gravel and sand
Sand and gravel
Medium to fine sand, silt
Soft blue-gray clay
(lake sediments)
No rock
Sand, gravel
Blue "clay" (silt)
Sand, gravel
Gray silt ("tough blue clay")
no rock
Sand , gravel
Gray silt, some sand, gravel
Fine sand, silt
Gray silt, trace sand, clay, gravel
Fine to medium sand, some silt
Gray silt with increasing gravel
of depth (till)
Rock
Depth
(meters)
from
0
12.5
17.7
17.8
0
10.4
17.4
0
0
7.6
8.8
11.0
0
3.0
22.6
27.4
34.1
46.0
65.8
to
12.5
17.7
17.8
32.3
10.4
17.4
22.9
137
7.6
8.8
11.0
37.2
3.0
22.6
27.4
34.1
46.0
65.8

       111-17

-------
GE (MORPHOLOGY

    Although the  distribution  and  stratification of glacial deposits are
major influences  on  the hydrologic characteristics of the Mill Creek basin,
the bedrock structure  also  controls the general basin configuration and the
current trends  of  individual streams or stream segments.   The resistant
sandstone  (Portage Escarpment  of Mansue,  Young, and Soren,1983) that
trends east-west  between Rogersville and  Patchinville (fig. 3) was a signif-
icant barrier to  the advancing ice sheets.   Several glaciations strongly
eroded the escarpment, producing prominent  drift-filled strike valleys
trending east-west along the weaker rock  layers at the foot of the escarp-
ment.

    During the  glacial readvance to the Valley Heads Moraine, the ice front
became lobate,  as  indicated by the position of moraines and ice-marginal
drainage channels  (fig* 3).  In figure  3,  the  ice positions marked as
stages 3 and 4  correspond to the classic  "Valley Heads" readvance; the other
ice positions have been inferred by Connally (New York State Geological
Survey, written coramun., 1961)  to  represent older recessional moraines.
All moraines and  outwash deposits  associated with these ice positions have
modified the terrain and influenced the modern hydrologic regime of the
Mill Creek subbasin.  For example,  headwater tributaries  originating on the
thinly covered  bedrock divides were impeded or diverted downstream on the
valley slopes by  the various moraines,  outwash gravel, ice-marginal chan-
nels, and kame  terraces.  The  modern drainage  pattern has resulted from the
modification of these older glacial landforms.  Some tributary drainage
follows ice-margin channels and skirts  the  edges of moraines.  The deep
incision by Mill  Creek through the Valley Heads Moraine permits observation
of the relationship between glacial stratigraphy, georaorphology, and
ground-water movement.

    In summary, the sequence of repeated  ice retreat and  readvance has pro-
duced a stratigraphy and morphology favorable  to significant ground-water
recharge in the upper basin.   The  low relief of the glacial moraines and
the swampy depressions on the  broad floor  of the former lake basins near
Wayland enhance recharge to the underlying  permeable outwash gravel and
sandy till.
                                    111-18

-------
                                 SECTION 5

                             STONY  BROOK BASIN
GEOLOGY

    The physiographic and  geologic  setting of Stony Brook is similar to that
of Mill Creek except that  Stony  Brook  flows directly down the Portage
Escarpment, across  the Valley  Heads Moraine near Stony Brook Park, and into
Canaseraga Creek 1.4 km  above  the  confluence of Mill Creek.  It is a smaller
subbasin, and the stream is  not  diverted through a broad drift-filled valley
as Mill Creek is.

    Ice associated  with  moraine  positions 1 and 2 (fig. 3) must have filled
the upper reaches of Stony Brook subbasin, as indicated by the sand, gravel,
and kame deposits along  the  divide  on  the south margin of the basin above
South Dansville  (fig. 2).  However, exposures of glacial sediments in this
basin upstream from Stony  Brook  Park are poor,  and the map units are largely
extrapolated from reconnaissance field mapping on aerial photographs.

    Surficial deposits in  the  basin consist of thin, stony to sandy till in
the uplands and  poorly exposed sand and gravel beds along the lower stream
courses.  From a few exposures,  bedrock is inferred to be near the surface in
most streambeds  but veneered with  grayish to brown (oxidized) till and outwash
or alluvium in most of the area.

    For 1.6 km downstream  from South Dansville, the streambed has extensive
till exposures with silt,  sand,  and gravel along the valley sides.  Because
the main Valley  Heads readvance  did not extend this far south, these deposits
differ in origin and texture from  those on Mill Creek in the section between
Stone Falls and  Perkinsville.  However, the upper Stony Brook subbasin has
relatively permeable glacial sediments at the surface to absorb precipitation
and also seems to have a veneer  of  clay-rich till over bedrock, which reduces
ground-water infiltration  into bedrock.  This situation, as in the Mill Creek
basin, produces  slumping.


GEOMORPHOLOGY

    Although it was not  possible to correlate all ice-front positions from
Mill Creek into  the Stony  Brook  basin, an approximation of ice positions was
made from extrapolation  of the ice-front elevations.  It seems probable that
the moraine in the  upper parts of  the  Stony Brook subbasin is equivalent to
ice position 1 in figure 3.  The basin's small size and high altitude pre-
vented a large ice  lobe  from extending southward into the basin.  Prominent


                                    111-19

-------
                                                  77 37'30"
                                   V         I  •» ' I

                                  i\*KW<
                           Otlet to north at Pearl Creek west of Geneseo,
                           dashed v^harf atonpnmet0tY

                                    channej for indicated stage
             Base from U.S. Geological Survey
             Tvi-minute auadfangT*!, 1B7B
Figure 3.  Ice-Margin positions of latest glaciation in Canaseraga Creek,
                        111-20

-------
77 37'30'
                                           Glacial a»oloav by ft.A. Voung. 1977
  Stony Brook,  and Mill Creek areas near  Dansville.
                                        111-21

-------
moraines such  as  those  near  Perkinsville and Patchinville are absent  in  the
Stony Brook  subbasin.   In addition,  because drainage along the ice margin
could not cross over  the  higher divides south of South Dansville, the valley
sides in the Stony  Brook  basin contain much less outwash sand and gravel in
the form of  kame  terraces than in the Mill Creek subbasin.  In other  words,
the lack of  thick glacial outwash deposits in the Stony Brook area above Stony
Brook State  Park  reflects the lack of major through-flowing meltwater streams.
The thinner  deposits  consist predominantly of sediments produced by local
melting of debris-laden ice.
                                    111-22

-------
                                 SECTION 6

                      UPPER CANASERAGA CREEK SUBBASIN

     Canaseraga Creek begins near the Livingston-Allegany County line  (fig.
 1)  and  flows  southeast,  then east,  and finally turns northeast into the
 broad drift-filled valley south of  Dansville before crossing the Valley
 Heads Moraine in the vicinity of Poags Hole near the Livingston-Steuben
 County  line.   From Dansville northward to the Genesee River, the Canaseraga
 flows through the  glacially widened and deepened southern extension of the
 ancestral  Genesee  Valley.  Because  the lower subbasin (Canaseraga Creek
 flood plain)  differs considerably from the upper basin, it is discussed
 separately in the  next  chapter.
GEOLOGY

    Upstream  from the  town of  Canaseraga (fig. 1), the creek channel is
confined  to a narrow valley that was formerly the meltwater outlet for
Valley Heads  ice  south of  Nunda.  This 13-km reach extends mostly over
outwash that  was  deposited as  the Valley Heads ice was melting and
discharging meltwater  southward toward Arkport.   From 1.6 km northeast of
Canaseraga to Stony  Brook  State Park,  the stream has incised 35 to 90 m
downward  into a moraine complex 6.4 km wide formed by the Valley Heads
readvance south of Dansville.

    The glacial stratigraphy along Poags Hole is similar to that along Mill
Creek above Stone Falls.   A gray clay-rich basal till is overlain by
massive silty sediments and capped by  the sandy  brown till of the most
recent Valley Heads  readvance.   Younger deltaic  and fluvial sediments cap
some stream divides.

    Along the steep  valley eroded through the moraine at Poags Hole, slumps
are evident along the  valley sides in  the unstable massive silt as well as
in the basal  till.   Because the section through  Poags Hole has a flood
plain 600 to  900  m wide, some  of these slides are at a distance from the
creek and do  not  feed  sediment  directly into the main channel.

    Just above where the stream enters the wide  valley at Dansville, it is
constrained by bedrock along the west  side of the old buried glacial
valley.  This bedrock  prevents  active  downcutting of the channel and thus
forms a local base level for the upstream reach  through Poags Hole.  Bed-
rock also constricts the channel along a series  of waterfalls 3 km below
Canaseraga.   The  gradient  is approximately 9.5 m/km through the Poags Hole
section between the  constrictions.   Like both Mill Creek and Stony Brook,
Canaseraga Creek  seems  to  derive most  of its sediment from silt and till
                                     111-23

-------
along the channel wherever  it  is  incised through morainal deposits of
Valley Heads age.  A series  of  large active slides in these materials is
present along  the valley walls  at Stony Brook State Park along both
Canaseraga Creek and lower  Stony  Brook.  In the spring, mud slides and
slurries have  been seen flowing into the Canaseraga from reactivated parts
of old landslides on the west  side of the valley.  Even when the slides are
not contributing large amounts  of sediment, the streams become noticeably
more sediment  laden  downstream  from the older slide scars.
GROUND WATER

    Discharge of  ground water  plays an important role in the transport of
sediment to streams.   Ground water from the upper basin probably emerges
into the stream in  large  quantities near the bedrock and till exposures
just downstream from  the  town  of  Canaseraga.  Water moving through the silt
overlying  the basal till  causes  instability and large slumps that are
active intermittently throughout  the Poags Hole area.  Tilted trees, slide
blocks, and irregular terrain  along the valley sides attest to slope move-
ment throughout the 10-km valley  section incised through the moraine.  The
deepening  and widening of this valley segment is undoubtedly a result of
this type  of slump  failure during channel downcutting.  Below the falls,
where bedrock does  not limit downcutting, the channel has been deepened 30
m within a 2.4-km reach.   No tributaries enter the stream along that reach.
This difference in  channel shape  attests to the rapid erosion of the
glacial deposits  and  supports  the hypothesis that streambed erosion and
valley widening by  slope  failure  have been major contributors to suspended
sediment in this  and  similar basins.

    The coarse outwash gravel  south of the moraine near Poags Hole should
form an even better ground-water  recharge unit than the deposits near
Wayland, but neither  the  thickness of the outwash nor the movement of
ground water could  be determined  from available information.
GEOMORPHOLOGY

    The  lobe of  ice  from the Valley Heads readvance southwest of Dansvilie
encountered  less resistance than the lobes at Wayland and Stony Brook
because  of a preexisting north-south valley that allowed passage and pro-
vided an unobstructed  outlet for outwash deposits and meltwater.  For  this
reason,  the massive  moraine at Poags Hole has only 12 to 18 m of surface
relief and grades almost imperceptably into an outwash fan (valley  train)
extending southward.  The reach of Canaseraga Creek from Canaseraga to
Stony Brook  State Park was probably incised originally from a semicircular
course around  the front (south) edge of the main moraine and through low
swales across  the moraine toward Dansville.  A more direct southerly route
was apparently blocked by a large outwash fan deposited by meltwater dis-
charging from  the narrow bedrock channel northwest of Canaseraga.   It  is
also possible  that the upper reach of Canaseraga Creek (west of the town of
Canaseraga) was  formerly a tributary to the main valley leading south  from
Poags Hole but was captured by headward erosion from the direction  of  Poags
Hole.

                                    III-24

-------
    The upper Canaseraga  drainage  basin is more complex than the Mill Creek
basin.  The moraine deposits,  although more extensive than those in the Mill
Creek basin, have more  subdued relief  and  a different depositional history
resulting from the large  breach eroded in  the Portage Escarpment.  The
moraines in the valley  near Wayland  are lobate with small marginal outwash
channels.  The moraine  at  Poags Hole is more massive, lacks distinctive
lobate ridges, and is veneered with  coarse outwash gravel deposited by
large volumes of meltwater that did  not discharge directly Into a lake.
Gravel pits in glacial  outwash south of the Poags Hole moraine contain
thick sections of very  coarse  cobble gravel.

    The kame moraine in the valley east of Canaseraga is responsible for
the distinctively curved  shape of  the  Canaseraga Creek channel where it
parallels the moraine margin.   The lack of tributaries can be attributed  to
the high permeability of  surface deposits.  The upper Canaseraga, from its
headwaters to Dansville,  is an example of  a stream that conforms basically
to former glacial valleys  and  ice-contact  depositional relief.
                                   111-25

-------
                                 SECTION 7

                       CANASERAGA CREEK FLOOD PLAIN
GEOLOGY

    During preglacial  time,  the  broad flood plain of lower Canaseraga
Creek, now 2.4 to 4.0  km wide, was  the main trunk of a large stream to
which the Genesee River was  tributary.  It is believed that the Genesee
River, before glaciation,  flowed from Portageville to Sonyea through the
present Keshequa valley (fig.  1), then into the main trunk stream in the
Canaseraga valley.   Subsequently, glacial drift blocked the course of the
Genesee River and rerouted the flow from Portageville to Mount Morris (f^.g»
1) through Letchworth  State  Park (Fairchild,  1926).  The lower Canaseraga
valley was more extensively  scoured than the  upper part because its axis
was alined north-south, in the direction of ice movement.

    The lower part of  the  valley is inferred  to have contained a shallow
lake dammed by a glacial moraine that plugged the Genesee Valley 35 km
north of Dansville near Geneseo  about 11,000  years ago.  As the Genesee
River cut through the  moraine, lowering the outlet, the lake began to drain
and fill in with peat.  The  Genesee River deposited an alluvial fan or
delta (12 m thick) near Mt.  Morris  that may have been an additional control
on the lake level and  (or) sediment-accumulation rate in the valley.  The
periodic buildup of  the delta  fan in the valley near Mt. Morris would dam
the river temporarily, creating  a shallow lake extending south to Dansville.
The temporary ponding  of water in this area would form an effective sedi-
ment trap for the many small tributaries draining the valley walls.

    The surficial material of  the lower Canaseraga valley gradually changes
northward from sandy deltaic and lacustrine sediments at Dansville to gray
lacustrine clays and silts and marsh deposits consisting of peat and muck
near Keshequa Creek  at Sonyea  (fig.  1).

    Radiocarbon age  determinations  on peat horizons collected from flood-
plain borings along  Interstate Highway 390 (Young, 1977) indicate a
transition from a shallow  open lake  to periodically flooded marsh areas
about 11,000 years ago.  (See  table  10.)  Peat layers of varying extent and
thickness are scattered throughout  the valley from near present land sur-
face to depths of 10 m.  The thickest layers  occur at depths between 1.5
and 3.0 m and between  7.6  and  9  m below land  surface.  Underlying the marsh
deposits at a depth  of 9 to  10 m is  a lacustrine silty clay that is notice-
ably varved at a depth of  14 m;  this layer may be a few hundred meters
thick.
                                    111-26

-------
    Although  the Canaseraga  valley has  accumulated  a net  of 10 m of  sedi-
ment In the last 11,000 years,  cyclic periods  of  degradation and aggrada-
tion probably occurred as a  result of climatic variations.   Holocene
climates throughout North America have  undergone  several  alternations from
cool and moist  to warm and dry.  Aggradation  typically  occurs during warm,
dry periods, whereas degradation occurs during cool,  moist  periods.
Recently obtained dates from buried hearths and soil profiles near Geneseo,
about 3.1 ,km northeast of Mt. Morris, Indicate that the flood plain  has
undergone 1.2 to 1.8 m of aggradation in the  last 400 years (Mansue, Young,
and Soren, 1983).
GROUND WATER

    The role of ground water  In creating unstable  stream-bank conditions
and high sediment loads  is  less significant  along  the  Canaseraga flood plain
than In the headwater subbasins.  Because  the  flood  plain lacks  steep banks
of glacial material, slumping and similar  phenomena  associated with ground-
water seepage are less likely to occur.

    The coarse deltaic sediments near Dansville  should form an excellent
recharge area and permit ground water to move  readily  northward  Into the
Canaseraga flood plain at depths generally less  than 10 m.   Relatively
impermeable clay or silt at shallow depths would prevent rapid infiltration
of ground water to deeper sediments.  Fine sediments of low permeability
are known to extend to depths of at least  73 m.  Water levels in borings
generally range between  2.4 and 9.1 m below  land surface;  borings with per-
forated casing below 15-m depths show decreasing amounts and rates of
seepage from the fine silt and clay.

    From these observations,  It seems likely that  most of the water from
the Canaseraga basin enters the Genesee River  either in the main channel or
as ground water at or above present channel-bottom elevations.   This would
imply that streamflow measurements on Canaseraga Creek include most of the
water moving out of the basin because little ground  water is likely to be
moving at through the fine-grained lacustrine  sediments.
                                 111-27

-------
                                SECTION  8

                              SEDIMENTATION

    Fluvial sediment can be divided  into two  general categories—bedload
and suspended load.  Bedload  consists  of soil,  rock particles, and other
debris that rolls or skips along  the streambed;  suspended sediment includes
mineral, colloidal, and organic material that is kept in suspension by tur-
bulence.

    Streamflow, suspended sediment,  bed  material, and source material were
measured during the collection period,  1975-77;  the stations and period of
collection are listed  in table 3.  Detailed studies were made to identify
source materials, describe sediment  transport,  and discuss the nature and
susceptibility of sedimentary deposits  to  erosion.

    Suspended-sediment load and yield  for  stations in the Mill Creek sub-
basin, at the Stony Brook site, and  other  sites in the Genesee River basin
are reported by Mansue and Bauersfeld  (1983 - table 7).
DATA COLLECTION

    The steamflow and  sediment-measurement sites on Mill Creek and Stony
Brook were selected  on the  basis  of  a reconnaissance of geologic setting,
available suspended-sediment  information,  and site accessibility.  Gages
equipped with continuous  stage  recorders and automatic water samplers were
installed at sites where  relatively  high suspended-sediment loads were
indicated.  One  site was  along  Mill  Creek at Knox Street in Dansville; a
second was at Stone  Falls Road  near  Dansville.  A partial-record site
upstream on the  main stem at  Patchinville was used, and another was
established near Perkinsville.   In addition, two miscellaneous measurement
sites were established on Little  Mill Creek at County Line Road and at the
New York State Route 63 bridge  near  the mouth.  Location of these sites is
shown in figure  1.
SUSPENDED-SEDIMENT  TRANSPORT IN SUBBASINS

    During  low  flow and  base flow,  field observations and suspended-
sediment measurements  of Mill Creek from the headwaters to Perkinsville
revealed relatively clear water.   However, where the stream enters the
canyon below  Perkinsville,  it turns milkly gray, mainly from gray muddy
slurries created  by springs issuing near the contact between the dense gray
basal till  and  the  overlying fluviolacustrine deposits.  Some channel ero-
sion must also  contribute to the  suspended-sediment load at low flow.

                                    111-28

-------
TABLE 3.  STATIONS  AT  WHICH STREAMFLOW AND SUSPENDED-SEDIMENT WERE MEASURED
          IN THE  CANASERAGA CREEK BASIN,  WITH DATES OF DATA COLLECTION

                     [Locations  are shown in figure 1.]

Station number and name
04224740

04224775

04224848

04224900

04224930

04224940

04224978
04225000


04225500


04225600

04225670
04225915
04225950

04226000


04227000


04227500

Sugar Creek near
Canaseraga
Canaseraga Creek
above Dans vi lie
Stony Brook at Stony
Brook State Park
Mill Creek at
Patchinville
Mill Creek at
Perkinsvllle
Mill Creek near
Dansville
Daily record
Streamflow Sediment

—

8/74-9/77

—

—

—

—
Mill Creek at Dansville
Canaseraga Creek near
Dansville

Canaseraga Creek at
Grove land

Bradner Creek near
Dansville

7/70-9/76,
7/10-9/35

10/56-9/64,
3/11-10/19

—
Bradner Creek at Sonyea
Keshequa Creek at Nunda
Keshequa Creek at
Tuscarora
Keshequa Creek at
Sonyea

Canaseraga Creek at
Shakers Crossing

Genes ee River near
Mount Morris

—

11/74-9/77,
3/11-9/32

10/74-9/77, 3/75-9/77
11/59-9/70

6/03-9/77 4/75-9/77
Partial
Streamflow

2/75-9/77

—

12/74-9/77

7/76-9/77

7/76-9/77

7/76-9/77
12/74-9/77

12/74-9/77


12/74-9/77


12/74-9/77
12/74-9/77
12/74-9/77

12/74-9/77

—


—


—
record
Sediment

2/75-9/77

12/74-9/77

12/74-9/77

7/76-9/77

7/76-9/77

7/76-9/77
12/74-9/77

12/74-9/77


12/74-9/77


12/74-9/77
12/74-9/77
12/74-9/77

12/74-9/77

12/74-9/77


—


—

Note:  Refer to text for definition  of  station type.
                                     111-29

-------
     Stony  Brook has  a higher suspended-sediment discharge per unit stream-
flow than  Mill  Creek (Mansue and  Bauersfeld, 1983 - table 3).  In
small  basins  such as Mill Creek and Stony Brook,  the entire drainage area
may  be  affected by a single  small rainstorm.   Commonly, a large part of the
basin will receive equal quantities and intensities of rainfall at the same
time, particularly during winter  storms.   To  correlate the sediment loads
at adjacent sampling sites with the load  of Mill  Creek at Dansville,
suspended-sediment data collected at these sampling sites have been tabu-
lated  (table  4).   In table 4,  the storm data,  stream discharge, and
sediment-load data collected at these sites from  July 1976 to September
1977 are presented.   It is assumed that these  data represent yields from
generally  equal precipitation throughout  the  basin.

     The average suspended-sediment concentration  was the greatest at Stone
Falls, which  confirms  that the major sources  of sediment to Mill Creek are
derived from  the  reach from  Perkinsville  to Stone Falls.

     The predominant  factors  determining the suspended-sediment yield at
Patchinville  are  the rainfall intensity and the degree of soil saturation.
During storms of  low intensity, such as on April  23, 1977, when 5.1 cm of
rain fell  uniformly  over a 23-hour period, suspended-sediment discharge was
9.4  metric tons.   The  average streamflow, 0.74 m3/s, was relatively small
for  the amount  of precipitation.

    During a  storm of  high intensity,  such as  that of July 6, 1977, the
Arkport precipitation  gage recorded 2.8 cm in  1 hour, and a total of 3.6 cm
fell that  day.  However,  a slightly greater suspended-sediment discharge
resulted then than during the storm of April  23.   Approximately 24 hours
later  (July 7),  another 2.8  cm of rain fell within an hour (a total of 3.3
cm for the day).   The  ground was  saturated from the previous day, and the
instantaneous peak streamflow on  July 7 was 13.1  m3/s as compared with 0.68
n»3/s on July  6.   Similarly,  average streamflow during the July 7 storm was
8.7  times  greater than during the July 6  storm, although both had approxi-
mately the same  intensity and volume of precipitation.  The suspended-
sediment load on  July  7 was  260 times greater  than on April 23 and 174
times greater than on  July 6.   These antecedent soil conditions are an
important  factor  in  the availability of suspended sediment.

    The average  suspended-sediment discharge was  generally higher down-
stream at  Perkinsville than  at Patchinville during low- and moderate-
intensity  storms.  During high-intensity  storms,  deposition occurred in the
reach between these  sites.   Afterward, the lower  streamflows incorporated
this new material, resulting in the higher suspended-sediment transport
at Perkinsville.

     Sampling  during  the high-intensity storms  of  July 7 and September 19
revealed both higher suspended-sediment concentrations and higher sand
concentrations  at Patchinville than Perkinsville.  The lower suspended-
sediment yield  at Perkinsville is attributed  to the relative flatness of
the  broad  Wayland valley and the  poor drainage between these sites.  The
low  stream gradient  of 22 m/km in this section would be a significant fac-
tor  directly  related to the  sediment concentration, discharge, and
particle-size distribution.

                                     111-30

-------
    Suspended-sediment  loads are greater at the station near Dansville than
at the  other  site  because  the ravine downstream from Perkinsville contrib-
utes a  major  source  of  sediment, and the gradient (28 m/km) is relatively
high.   The  sediment  originated at the sides of the stream channel, where
slumps, mud flows, and  springs form at the contact between the relatively
impermeable dense  gray  till and the more permeable overlying deposits of
deltaic sand  and gravel, silty sandy till, and fluviolacustrine silt.

    The suspended-sediment discharge per km2 at Dansville was slightly less
than upstream at Stone  Falls, partly because of dilution by the inflow of
Little  Mill Creek  below Stone Falls.  Random samples and storm samples
collected on  Little  Mill Creek above the reservoir and near the mouth both
indicated low suspended-sediment concentrations, which may reflect the
gentle  rolling topography  of the drainage area, the permeability of the
surficial deposits,  which  consist of sandy till and patches of sand and
gravel, and the fact that  approximately two-thirds of the basin outflow
empties into  the reservoir, which would act as a sediment trap.  The chan-
nel from the  reservoir  outflow to the mouth is incised in relatively
resistant bedrock  and contributes only small amounts of sediment.  The few
stream  tributaries along this bedrock channel and the armor of cobbles over
dense gray  till between the station near Dansville and the station at
Dansville account  for the  reduced suspended-sediment yield within this
reach.
INTERSTATION  CORRELATION

    To  compare  the  sediment  load measured at different stations realisti-
cally,  the  suspended-sediment load for each storm at each station was
divided by  the  drainage  area.  The resulting data (suspended-sediment
yields) were  used to develop relationships between each subbasin and Mill
Creek at Dansville.  Figure  4 depicts the relationship between the
suspended sediment  yields  from these sites.  A straight-line relation on
log-log paper was assumed, and the best relationship was computed by the
least-squares method.

    The relationships  developed for the Patchinville and Perkinsville sites
are grouped below the  line of equal sediment yield.   The straight line
representing  the relationship is expressed by its slope.  The Patchinville
site has the  steepest  slope,  probably because of high sediment availability
during  the  higher flows  from this headwaters site.  The slope of the rela-
tionship for  the Perkinsville site is low and below the line of equal
yield,  mainly because  the drainage area upstream from this site is shallow
and has extensive wetland areas.   The curve for the site near Dansville is
completely  above the line of equal yield, which indicates a relatively high
amount  of suspended sediment in transport relative to the site at
Dansville.  This is attributed to the large source of sediment from the
Mill Creek  ravine between Perkinsville and this site.

   The  Stony  Brook  curve lies significantly above the line of equal yield
during  low  and  moderate  flows,  but at high flows the relationship is below
this line,  which suggests a  proportionally limited sediment supply.


                                      111-31

-------
          TABLE 4.  SUMMARY OF STREAMFLOW AND SUSPENDED SEDIMENT IN
                    MILL CREEK AND STONY BROOK BASINS, 1976-77

Date
Precipitation
intensity^-
Average
streamflow
(m3/s)
Mean
suspended-
sediment
concentration
(mg/L)
Suspended-sediment
Load
(metric
tons)
Yield
(metric
tons/km^)
MILL CREEK AT PATCHINVILLE. Drainage area 13.0 tan2;
                            percent of total drainage area  14;
                            average gradient 18 ra/km.
7/29/76
12/07/76
3/23/77
3/28/77
4/23/77
6/25/77
7/06/77
7/07/77
9/18/77
9/19/77
9/24/77
9/26/77
Average
MILL CREEK


7/29/76
12/07/76
3/23/77
3/28/77
4/23/77
6/25/77
7/06/77
7/07/77
9/18/77
9/19/77
9/24/77
9/26/77
Average
High
Low
Low
Low
Moderate
Moderate
High
High
Moderate
High
Moderate
Low

AT PERKINSVILLE .


High
Low
Low
Low
Moderate
Moderate
High
High
Moderate
High
Moderate
Low

.71
.25
.40
.45
.74
.20
.34
2.97
.71
4.05
1.10
.82
1.06
Drainage area 46
percent of total
average gradient
_—
.68
—
1.7
2.0
.71
.68
3.0
—
4.98
4.67
3.54
2.4
213
10
59
62
84
42
325
3880
105
1005
167
84
503
.9 km2;
drainage
22 m/km.
„
62
—
47
150
110
176
1060
—
346
312
59
258
21
.23
3.08
3.6
9.4
.84
14
2430
7.7
766
20
6.6
274

area 50;

„_
4.1
-._
7.0
30
7.6
13
375
.._
197
137
18
88
1.6
.017
.24
.28
.73
.065
1.05
187
.59
59
1.54
.51
253



__
.087
__
.15
.64
.16
.27
8.0
—
4.2
2.9
.39
1.9
1 low, <0.5 cm/h
  moderate, 0.5-1.3 on/h
  high, >1.3 cm/h
                                    111-32

-------
                           TABLE 4  (continued).
Date
Precipitation
intensity1
Average
streamf low
(m3/s)
Mean
suspended-
sediment
concentration
(mg/L)
Suspended-sediment
Load
(Metric
tons)
Yield
(Metric
tons /km2)
MILL CREEK AT STONES FALLS. Drainage area  57.0 km2;
                            percent of  total  drainage  area  61;
                            average gradient  28  m/km.
7/29/76
12/07/76
3/23/77
3/28/77
4/23/77
6/25/77
7/06/77
7/07/77
9/18/77
9/19/77
9/24/77
9/26/77
Average
MILL CREEK

7/29/76
12/07/76
3/23/77
3/28/77
4/23/77
6/25/77
7/06/77
7/07/77
9/18/77
9/19/77
9/24/77
9/26/77
Average
High
Low
Low
Low
Moderate
Moderate
High
High
Moderate
High
Moderate
Low

AT DANSVILLE.

High
Low
Low
Low
Moderate
Moderate
High
High
Moderate
High
Moderate
Low

1.27
.963
—
1.81
2.10
.91
1.27
3.09
1.47
6.06
4.87
2.92
2.43
Drainage area 93.0
average gradient
1.76
1.05
.91
1.90
2.63
1.05
1.95
6.23
2.49
13.3
7.48
4.05
3.73
627
150
—
436
721
283
1100
6240
647
6080
2750
990
1820
km2;
23 m/km.
581
134
279
402
518
246
510
4380
476
4800
2020
718
1260
88
14
—
68
136
24
142
1630
93
3560
1440
237
676


111
14
23
68
138
24
143
2370
109
6220
1540
255
918
1.54
.24
—
1.2
2.4
.42
2.5
28.6
1.6
63
25.3
3.8
11.9


1.2
.15
.24
.73
1.48
.26
1.54
25.5
1.2
67
17
2.7
9.9
STONY BROOK AT STONY BROOK
  STATE PARK.
Drainage area 53.9 km2;
percent of total drainage area 92;
average gradient 27 m/km.
10/20/76
3/04/77
3/28/77
4/23/77
5/04/77
9/19/77
9/26/77
__
—
Low
Moderate
—
High
Low
5.0
2.6
2.7
6.6
2.8
10.9
3.8
896
114
194
655
184
1100
573
897
30.1
48.5
284
78.6
1685
234
16.6
0.56
0.90
5.27
1.46
31.3
4.34

                                     111-33

-------
            A Mill Creek at PatchmviMe
            B Mill Creek at Perkmsville
         •  C Mill Creek near Dansvitle

         O  D Stony Brook at Stony Brook State Park
0.01
                          1                .       10
             SUSPENDED-SEDIMENT YIELD OF MILL CREEK AT DANSVILLE. N.Y.
                      IN METRIC TONS PER SQUARE KILOMETER
Figure 4.—Suspended-sediment  yield  at Mill Creek and  Stony
             Brook stations in relation to yield at Mill  Creek
             station at  Dansville, July 1976  to September 1977.
                                 111-34

-------
 However,  this observation is inconclusive because data were available from
 only  four storms.

    Streamflow records in this part of New York indicate that the
 Canaseraga Creek basin has an average of 12 significant storms per year.
 The sum of suspended-sediment yield during 12 storms from July 1976 to
 September 1977 (table 4)  is considered to represent an average annual load.

    To  use the average annual load for a quantitative estimate of annual
 suspended-sediment  load,  any trend in suspended-sediment discharge for the
 entire  basin is assumed uniform throughout the subbasins.  Accordingly, the
 relationship between sediment yield at Dansville and each subbasin (fig. 4)
 may be  used to compute subbasin sediment yield; for example, a suspended-
 sediment  yield of  4 metric tons at Dansville yields a computed annual
 suspended-sediment  yield  of 5.3 metric tons per km2 for the station near
 Dansville.

    To  describe the relationship between each station and Dansville, table
 5  includes the standard error of an estimated yield and coefficient of
 determination from  the linear least squares relationships of log trans-
 formed  data (Draper and Smith,  1966,  p.  14).  A perfect fit would be
 obtained  if the coefficient equaled 1; at the site near Dansville the coef-
 ficient is 0.996.   This is probably a result of its proximity to the site
 at Dansville.   The  standard errors of estimate have been expressed in log
 units above and below the average regression line.  A standard error may be
 thought of as  the maximum error expected for a mean yield about two-thirds
 of the  time.   For example, the  error  for the mean sediment yield at
 Perkinsville  (10 metric tons) for nine storms is 4-2.9 metric tons per
 km2 an
-------
     The  relatively large standard error of suspended-sediment yield rela-
 tions  for  the  Patchinville station nay be partly explained by the degree of
 error  in (a) determining a runoff hydrograph from a few gage-height
 readings,  and  (b)  directly comparing data without adjustment for slight
 variations  in  rainfall distribution.  The total number of storm discharges
 available  for  comparison ranges from 12 at the Dansville station to 4 at
 Stony  Brook.

     Taking  the value of the suspended-sediment yield for each hydrologic
 event  for Mill Creek at Dansville, and entering the slope of the line of
 the  average  relationship (fig.  4), a computed suspended-sediment value is
 obtained for each  subbasin station and the Stony Brook station.  This value
 is tabulated,  and  the procedure is repeated for each storm at the Dansville
 station.  The  total  of the computed suspended-sediment yield for each sub-
 basin, multiplied  by the drainage area, is the suspended-sediment load.
 These  totals can be  expressed as a percentage of the total suspended-
 sediment load  passing Dansville and are tabulated in table 6 for each sub-
 basin  and for  Stony  Brook.

   Comparison  of the suspended-sediment load for each subbasin station
 (table 6) reveals  calculated annual suspended-sediment aggradation and
 deposition.  Subtraction of the load at the station near Dansville (7,850
metric tons) from  the load at the station at Dansville (11,070 metric tons)
 gives  3,220 metric tons,  obtained from the drainage area between these
 sites  (36 km2), Or 89 metric tons per km2.  Subtraction of the load at the
Perkinsville station (728 metric tons) from load at the station near
Dansville (7,850 metric tons) gives 7,122 metric tons, obtained from the
 increase in drainage area between these sites (10.1 km2), or 705 metric
 tons per km2.   This  high yield  is attributed to the unconsolidated
materials above the  dense gray  till in the Mill Creek gorge, described in
the  section "Mill  Creek Subbasin,  Geology."

     Subtraction of the load at  the Patchinville station (1,440 metric tons)
from the load  at the Perkinsville station (728 metric tons)  is -712 metric
 tons, with a drainage-area  increase of 33.9 km2.  This loss  indicates that
deposition has  taken place  between these sites, which may be attributed to
the  low gradients.

RESERVOIR SAMPLING

    The  sampling program permitted only sparse sampling of the Little Mill
Creek, the mouth of  which is between the station at Stone Falls and the
station at Dansville (fig.  1).   Samples were collected from  the bottom of
the  reservoir  on Little Mill Creek because sediment deposited in a reser-
voir generally  represents an integrated sample of upstream material.  The
perimeter was mapped and  seven  sites sampled within the reservoir to allow
interpretation  of  the differences  among sampling localities.  In addition,
location, depth, and nature of  the bottom samples were noted.  The seven
sites were selected  to represent  the reservoir bottom at the deepest loca-
tions.  The material sampled represents sediment deposited since the reser-
voir bottom was sealed with marl  in 1938.
                                     111-36

-------
TABLE 6.  MEASURED SUSPENDED-SEDIMENT YIELD AND LOAD OF MILL  CREEK  AT
          DANSVILLE AND COMPUTED SUSPENDED-SEDIMENT STORM YIELD  AND LOAD
          AT MILL CREEK AND STONY BROOK STATIONS.

                   (Drainage areas are in parentheses)

Mill Creek
at
Date of Dansville
event (93.0 km2)
7/29/76 1.2
12/07/76 .15
3/23/77 .24
3/28/77 .73
4/23/77 1.48
6/25/77 .26
7/06/77 1.54
7/07/77 25.5
9/18/77 1.2
9/19/77 67
9/24/77 17
9/26/77 2.7
Total yield,
metric tons/km2 H9
Total load,
metric tons 11,070
Percentage
of load at
Dansville 100

Mill Creek
Near
Dansville
(57.0 km2)
1.77
.26
.40
1.12
2.14
.43
2.22
30.0
1.77
73.3
20.6
3.74
137.8
7850
71

Mill Creek Mill Creek
at at
Perkinsville Patchinville
(46.9 km2) (13.0 km2)
0.35 0.55
.075 .045
.11 .079
.24 .303
.41 .710
.11 .087
.42 .74
3.38 22.0
.35 .55
6.92 71
2.51 13.5
.64 1.47
15.52 111
728 1440
6.6 13

Stony Brook
at State Park
(53.9 km2)
2.34
.57
.79
1.67
2.69
.83
2.76
18.5
2.34
35.5
14.0
4.04
86.0
4640
42

                                111-37

-------
     Particle-size and mineralogical analyses  were  done  on samples from
three locations.  Results are presented  in  following  sections.
PHYSICAL PROPERTIES OF SEDIMENT

    Selected physical properties  of  the  sediment  transported were eval-
uated, including suspended, bed,  and  source  materials.   Analyses included
particle-size determination on suspended sediment,  streambed samples,
source material, and Atterberg limits  of source materials.

Particle-Size Distribution

    The particle-size distribution of  suspended sediment from Mill Creek
and Stony Brook (average percentage)  is  presented in table  7.  The
suspended material transported during  1975-77  consisted of  13 to 23 percent
sand, 46 to 65 percent silt,  and  17  to 27 percent clay.  The percentage of
sand transported in suspension by a  stream is  generally in  direct propor-
tion to stream gradient and availability of  source material.  The highest
percentage of sand transported was at  the site on Mill Creek near
Dansville; this is because the channel upstream is predominantly sandstone,
and materials adjacent to the stream contain considerable sand.  Some
sorting would be expected during  transport.   Mill Creek at  Perkinsville had
a low percentage of sand owing to the  low gradient upstream.
    TABLE 7.  PARTICLE-SIZE  DISTRIBUTION OF SUSPENDED SEDIMENTS OBTAINED
              AT CANASERAGA  CREEK BASIN SAMPLING STATIONS, 1975-77

                         (All values  are average percent)
                                                   Particle size
                                           Clay         Silt       Sand
                                                     (0.004-     (0.062-
                                        «0.004 mm)  (0.062 mm)   2.0 mm)
Mill Creek at Patchinville
Mill Creek at Perkinsville
Mill Creek near Dansville
Mill Creek at Dansville
Stony Brook at Stony Brook State Park
22
—
22
17
27
65
—
46
60
59
13
13
32
23
14

                                    111-38

-------
Atterberg Limits

    As a part  of  the  source-material analyses, the erodability of
unweathered material  in areas adjacent to the streams was evaluated.  Shear
strength of soil  is considered a measure of its erodibility and can be
interpreted from  Atterberg limits analyses (L. H. Irwin, Cornell
University, written commun.,  1978).   Atterberg limits divide the cohesive
ranges of soils from  the solid to the liquid state into five stages
(limits) on the basis  of water content.   The tests are described by Means
and Parcher (1963, p.  70-83), and applications can be found in the current
literature.  The  liquid limit minus  the  plastic limit is defined as the
plasticity index  of the material. Material with a high liquid limit and
plasticity index  tends to be  more resistant to erosion.

    Four sample analyses that represent  material being actively eroded in
the Mill Creek basin  are shown in table  8.  The samples were collected from
the walls of a 30- to  45-m deep canyon that Mill Creek has eroded in the
Valley Heads Moraine  between  Perkinsville and Stone Falls.  The analyses
show relatively low liquid limits, plastic limits, and plasticity indices,
which indicate high susceptibility to erosion.  Rapid erosion of this
canyon on Mill Creek  contributes much of the sediment transported
downstream.
 TABLE 8.  ATTERBERG LIMITS  FOR GLACIAL MATERIAL ALONG MILL CREEK CANYON

  (Analysis by Cornell  University,  Department of Agricultural Engineering)
Material description
and date of sample
 Natural
 moisture
 content     Liquid  Plastic  Plasticity
(percent)    limit   limit	index
Lake sediment
(Oct. 7, 1977)

Till at base
of slump
(Sept. 30, 1977)

Gray till at base of  slump
at railroad cut
(sampling date not given)

Brown till 9 m
from surface
(Sept. 30, 1977)
   12.0
   13.4
   13.3
   18.6
14
19
19
20
12
12
12
16
                                   111-39

-------
MINERALOGY

    To compare  stream  sediments with  suspected source materials, suspended
sediment, bed material,  and  source  material  were  analyzed by X-ray diffrac-
tion.  Results  of  these  analyses  are  presented in table 9.  The suspended-
sediment samples included  sediment  transported during a variety of runoff
conditions.  Streambed material was collected after the seasonal high-flow
period, and  source materials were collected  at sites where material was
being noticeably eroded.

    The sampling is  from the postulated  major glacial deposits of various
ages.  Quartz,  illite, and chlorite were the major constituents of nearly
all samples.  Quartz was the predominant mineral  transported in all but the
lowest flows; this is  attributed  to its  prevalence and resistance to
weathering.  The shale,  siltstone,  and  sandstone  that underlie the basin
consist predominantly  of quartz,  and  most sedimentary particles in the till
and lake deposits were derived from these sedimentary strata close to the
study area.  Some of the material was probably glacially transported from
the Canadian Shield  and  older rocks to  the north.

    The major clay mineral constituents  were illite and chlorite.  These
noncomplex clays reflect a lack of  weathering owing to the relatively short
time since the  last  glacial  advance.  Till analyses for chlorite from the
Mill Creek basin along Highway 63 near Dansville  are comparable with the
percentage of chlorite found downstream  in the Canaseraga Creek samples
(Mansue, Young, and  Soren, 1983).

    The mineralogical  content of  samples from the reservoir on Little Mill
Creek was similar to that  of other  lake  sediments in the Genesee River
basin (Mansue,  Young,  and  Soren,  1983).
                                     111-40

-------
            TABLE 9.  MINERALOGICAL ANALYSIS OF SEDIMENT MATERIAL,
                      CANASERAGA CREEK BASIN, 1975-77

STATION I/ DATE
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224775
04224848
04224848
04224848
04224848
04224848
04224900
04224930
04224940
04224940
04224940
04224940
04224940
06-26-75
07-26-75
12-13-75
02-10-76
02-11-76
02-18-76
03-12-76
04-21-76
04-25-76
05-20-76
06-24-76
08-15-76
10-09-76
04-24-77
02-11-76
02-18-76
04-25-76
07-29-76
10-09-76
03-28-77
03-28-77
07-29-76
03-28-77
03-28-77
04-23-77
04-23-77
TIME
1700
1700
1200
—
—
1445
1330
—
1620
1200
1430
0515
1705
1630
__
0905
1130
1835
1615
1500
1440
1810
1500
1555
1915
1915
SIZE
MATERIAL 2/ MM 3/
STREAM BED
STREAM BED
STREAM BED
LOW FLOW
SUSPENDED
SUSPENDED
STREAM BED
LOW FLOW
HIGH FLOW
LOW FLOW
STREAM BED
AUTOM S.
HIGH FLOW
AUTOM S.
SUSPENDED
HIGH FLOW
HIGH FLOW
HIGH FLOW
HIGH FLOW
STREAM BED
STREAM BED
HIGH FLOW
SUSPENDED
STREAM BED
SUSPENDED
SUSPENDED
<0.062
>0.062
PSR
<0.062
<0.062
<0.062
<0.062
<0.062
—
<0.062
<0.062
PSR
PSR
PSR
<0.062
<0.062
—
PSR
PSR
<0.062
<0.062
PSR
PSR
<0.062
<0.062
PSR
MINERAL CONSTITUENT 4/
Q
35
66
31
38
39
36
59
26
57
36
56
22
58
43
41
49
39
40
49
65
58
46
47
43
46
52
P
19
6
6
12
8
4
9
5
14
7
6
6
6
4
9
13
8
6
7
-
10
8
12
11
28
4
K C
— _
- 8
2 8
5 4
1 «.
1 -
4 7
4 4
3 3
3 -
- 17
- -
- 9
15 8
1 -
13 -
- -
5 1
3 -
8 -
4 3
4 7
4 17
5 15
2 10
17 8
CL
46
20
53
41
52
59
21
61
23
54
21
72
27
30
49
25
53
48
41
27
25
35
20
26
14
19
IL
33
13
38
30
—
—
16
47
18
39
16
59
21
23
_
18
40
36
30
20
18
26
14
16
10
13
CH
13
6
15
11
—
—
5
14
5
15
5
13
6
7
__
7
13
12
11
7
7
9
6
9
4
5
KA
_
1
-
-
-
-
-
-
-
-
-
TR
-
TR
_
-
-
-
-
TR
-
_
TR
1
-
1
I/ STATION NUMBER REFERS TO LOCATION  ON FIGURE 1 AND TABLE 3
      EXCEPT THE FOLLOWING SITES:
      04224964 LITTLE MILL CREEK AT COUNTY  LINE ROAD NEAR DANSVILLE
      04224965 LITTLE MILL CREEK RESERVOIR  NEAR DANSVILLE

21 AUTOM S. » MATERIAL COLLECTED BY AUTOMATIC  SUSPENDED-SEDIMENT SAMPLER
         M  - METERS OF DEPTH BELOW WATER SURFACE

3/ PSR DENOTES PIPET PARTICLE-SIZE ANALYSIS RESIDUE

4/ Q=QUARTZ      P=PLAGIOCLASE  K=K-FELDSPAR   C-CALCITE     TR-TRACE
   CL=CLAY       IL=ILLITE      CH«=CHLORITE    KA=KAOHNITE
   ALL VALUES ARE IN PERCENT
                                     II1-41

-------
                          TABLE 9   (continued) .
                                         SIZE
MINERAL CONSTITUENT 4/
STATION I/   DATE  TIME    MATERIAL 2/   MM 3/   Q  P  K  C  CL  IL  CH  KA
04224964  03-28-77  1720  STREAM BED   <0.062   49 10  8  5  28  18  10
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224965
04224978
04224978
04224978
04224978
04224978
04224978
04224978
04224978
04224978
04224978
04225000
04225000
04225000
04225000
04225000
04225000
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225500
04225600
04225600
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
08-25-76
01-27-76
02-17-76
02-17-76
02-18-76
05-20-76
07-29-76
10-09-76
03-28-77
03-28-77
04-24-77
06-26-75
06-26-75
01-27-76
02-10-76
02-17-76
02-18-76
06-23-75
07-23-75
12-13-75
02-11-76
02-17-76
03-05-76
03-12-76
04-22-76
04-24-76
04-24-77
02-18-76
10-21-76
—
—
—
—
—
—
—
—
—
—
—
__
1525
1645
0930
—
1745
1555
1715
1715
1425
1720
1720
—
—
1330
—
1930
1930
0900
—
1810
1215
0900
1330
1830
0910
1015
1105
CORE01 . 5M
CORE<§1 . 5M
CORE01.5M
CORE@1 . 5M
CORE@2.3M
CORE@2.3M
CORE@2.3M
CORE@6.4M
CORE@6.4M
CORE@6.4M
CORE@6.4M
SUSPENDED
HIGH FLOW
HIGH FLOW
HIGH FLOW
LOW FLOW
HIGH FLOW
HIGH FLOW
SUSPENDED
STREAM BED
SUSPENDED
STREAM BED
STREAM BED
SUSPENDED
LOW FLOW
HIGH FLOW
SUSPENDED
STREAM BED
STREAMBED
STREAM BED
SUSPENDED
HIGH FLOW
RECESSION
STREAM BED
LOW FLOW
LOW FLOW
SUSPENDED
HIGH FLOW
SUSPENDED
<0.062
XJ.062
<0.062
>0.062
<0.062
>0.062
<0.062
<0.062
>0.062
<0.062
>0.062
<0.062
<0.062
<0.062
<0.062
<0.062
PSR
PSR
<0.062
<0.062
PSR
>0.062
<0.062
<0.062
<0.062
—
PSR
<0.062
>0.062
PSR
PSR
__
—
<0.062
<0.062
—
<0.062
<0.062
<0.062
65
60
59
59
56
49
53
47
46
51
42
40
59
60
49
43
44
38
41
39
42
66
48
36
42
56
43
34
59
46
37
66
54
56
40
59
40
54
28
5
11-
7
7
9
5
7
9
6
5
13
11
8
7
12
12
12
12
5
18
8
11
14
8
7
9
12
7
6
11
9
9
12
8
10
11
9
10
6
3 1
5 -
4 -
5 -
- -
3 -
4 -
— —
3 -
5 -
- 1
3 -
4 4
6 3
4 -
4 8
5 5
5 9
5 10
2 18
6 12
- 7
— —
1 -
4 2
3 5
4 -
— —
5 11
4 4
4 -
_ ._
6 -
_ _
3 3
_ ~
4 12
5 —
- —
26
24
30
29
35
43
36
44
45
39
44
46
25
24
35
33
34
36
39
23
32
16
38
55
45
27
41
59
19
35
50
25
28
36
44
30
35
31
66
19
17
23
23
27
33
29
32
33
30
34
.•._
18
17
26
24
25
27
27
17
22
12
27
— -
34
20
—
43
14
27
—
19
21
30
35
23
25
21
48
6
7
7
6
8
10
7
12
12
9
10
*•_
7
7
9
9
9
9
9
6
9
4
11
— —
11
7
— _
16
5
8
—
6
7
6
9
7
9
10
18
1
-
-
—
-
-
—
_
-
-
-
_
—
—
—
—
—
_
3
—
1
«(•
_
—
_
—
_
_
_
_
_
_
—
_
_
_
1
«.
—
                                   111-42


-------
TABLE 9   (continued).


STATION I/ DATE
04225670
04225670
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225915
04225950
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04226000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
04227000
07-17-75
' 04-25-76
__
—
07-19-75
07-19-75
01-14-76
02-09-76
02-17-76
03-04-76
04-23-77
01-14-76
__
—
06-26-75
06-26-75
06-26-75
12-13-75
01-14-76
02-11-76
04-22-76
06-25-76
04-23-77
06-26-75
07-08-75
07-17-75
07-23-75
09-26-75
09-26-75
12-13-75
01-13-76
02-19-76
03-12-76
04-25-76
10-21-76
04-23-77
04-24-77
04-25-77

TIME
._f .
1340
__
—
—
—
—
—
1035
1600
2000
1410
__
—
—
—
—
1550
1530
0900
0930
1045
1910
1915
1530
1915
1800
1040
1515
1615
—
0930
1600
1430
1230
1245
1050
0900


SIZE
MATERIAL 2/ MM 3/
STREAM BED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
SUSPENDED
LOW FLOW
HIGH FLOW
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
STREAM BED
STREAM BED
STREAM BED
STREAM BED
SUSPENDED
HIGH FLOW
LOW FLOW
STREAM BED
SUSPENDED
STREAM BED
LOW FLOW
STREAM BED
STREAM BED
HIGH FLOW
HIGH FLOW
STREAM BED
LOW FLOW
HIGH STAGE
STREAM BED
HIGH FLOW
SUSPENDED
SUSPENDED
SUSPENDED
SUSPENDED
<0.062
<0.062
<0.062
<0.062
<0.062
>0.062
<0.062
<0.062
—
—
<0.062
<0.062
<0.062
<0.062
< 0.62
> .25
> .062
PSR
<0.062
<0.062
<0.062
<0.062
<0.062
<0.062
0.062
>0.062
X3.062
<0.062
<0.062
PSR
—
<0.062
PSR
—
PSR
<0.062
<0.062
<0.062







MINERAL CONSTITUENT 4/
Q P
44 9
28 6
52 6
45 10
34 7
59 14
26 5
51 5
51 8
48 12
47 9
24 5
40 23
42 8
56 7
50 22
63 13
27 5
33 6
58 8
30 7
67 14
38 9
34 12
23 6
58 7
55 9
56 8
54 10
43 7
31 8
48 9
26 8
45 9
52 8
44 17
34 21
42 17
K
3
3
3
3
4
8
3
3
4
7
8
2
3
7
-
4
-
-
1
4
-
3
5
15
-
-
4
7
-
-
5
11
7
8
-
4
3
6
C
3
—
8
12
-
3
-
-
-
-
6
-
2
12
3
4
4
5
-
-
5
-
9
6
9
12
9
-
-
3
-
2
—
-
4
3
9
5
CL
41
63
31
30
55
16
66
41
37
33
30
69
32
31
34
20
20
63
60
30
58
16
39
33
62
23
23
29
36
47
56
30
59
38
36
32
33
30
IL
30
—
23
22
39
11
—
31
27
25
22
—
23
22
26
15
14
47
—
21
43
12
30
24
46
15
15
21
27
36
38
22
47
29
29
22
23
19
CH
11
—
7
7
16
5
—
10
10
8
7
—
7
8
8
5
6
16
—
9
15
4
8
9
16
5
8
8
9
11
18
8
10
9
7
8
8
9
KA
_
—
1
1
-
TR
-
-
-
-
1
-
TR
1
-
-
-
T
-
-
-
-
1
_
-
3
TR
-
-
-
-
-
2
-
-
2
2
2
         111-43

-------
                             TABLE  9   (continued).
LOCATION 5/
                 SIZE    MINERAL CONSTITUENT
DATE  MATERIAL 6/ MM   Q  P  K  C  CL  IL CH  KA
EMO RD, S. OF PATCHINVILLE 05-13-76 HLD  TILL <0.062  72   5  4  1  18  15  3  —
EMO RD, S. OF PATCHINVILLE 05-13-76 HLD  TILL X).062  66   5  3  -  26  22  4  —
MILL CR RAVINE, PERKINSVIL 04-02-76 LCS       <0.062  51  15  3 16  15   95   1
MILL CR RAVINE, PERKINSVIL 04-02-76 TBS       <0.062  44   7  4 16  29  22  7  —
RT 36, DANSVILLE           04-02-76 TILL     <0.062  33   8  5 29  25  18  7  TR
RT 63, DANSVILLE           04-02-76 V.CLAY    <0.062  45  11  5 13  26  17  8   1
RT 63, 1.4 KM E.OF DANSVIL 05-13-76 BR LAKE   <0.062  52  10  8  2  28  22  6  --
RT 63, 1.4 KM E.OF DANSVIL 05-13-76 BR LAKE   >0.062  56   7  -  3  34  29  5  —
5/ CR DENOTES CREEK
   E  DENOTES EAST
   RD DENOTES ROAD
   PERKINSVIL DENOTES PERKINSVILLE
   DANSVIL DENOTES DANSVILLE

6/ HLD TILL DENOTES HIGHLAND SANDY TILL
   LCS      DENOTES LACUSTRINE SILT AND  CLAY
   TBS      DENOTES BROWN SANDY TILL
   V.CLAY   DENOTES VARVED CLAY
   BR LAKE  DENOTES BROWN LAKE
                                    111-44

-------
                                SECTION  9

                  REGIONAL EROSION AND DEPOSITION  RATES
    To calculate erosion and deposition  rates  In  the  Canaseraga  Creek
basin, documentation of historic and prehistoric  changes  in the  stream and
flood-plain altitudes were sought.  Radiometric carbon-14 analyses  of organ-
ic materials from glacial and stream deposits  have  provided data on
general erosion and deposition rates back  to 11,000 years ago.   This date
shortly follows glacial recession.  The  geologic  ages and possible  signifi-
cance of three samples are listed  in table  10.

    Samples RAY-GS-9 and RAY-GS-10, obtained from approximately  9 m below
the present flood-plain surface, indicate  a transition of the Dansville-
Canaseraga valley from an open lake to a shallow, occasionally flooded
marsh about 11,000 years ago (table 10).   These and other samples analyzed
and described in Mansue, Young, and Soren  (1983) from  elsewhere  in  the
Genesee River basin indicate that  net sediment-deposition rates  for com-
bined Genesee River-Canaseraga basin streamflow into  this old lake  basin
(now Canaseraga valley) between 8,000 and  11,000  years ago were  probably
less than present sediment-transport rates.  These  sedimentation estimates
are long-term averages that include unknown variations caused by climatic
changes during the 3,000-year interval.  Modern sediment  transport  seems to
be nearly four times greater than  the amounts  needed  to account  for the
average increment of deposition during the  filling  of the old lake  basin.
However, this conclusion is valid  only if  it is assumed that the lower
Canaseraga basin was a shallow lake with a  restricted outlet during this
period, thereby trapping most of the sediment.  Analysis  of log  sample
RAY-GS-8 suggests that stream-channel migration has been  active  over at
least the last 180 years.

    In summary, the greatest erosion seems  to  be  occurring in headwater
areas where ground-water seepage causes  bank failure  in fine-grained stra-
tified deposits.  Modern sediment  deposition rates  in the Canaseraga flood
plain are probably greater than those during postglacial  times.
                                   111-45

-------
                          TABLE 10.  DATES FROM CARBON-14 ANALYSES, CANASERAGA CREEK BASIN

                                     (Samples  collected by R. A. Young and L. J. Mansue;
                                      Analyses by Teledyne Isotopes, Westwood, N.J.)
M
M
M
Laboratory
sample
no. 1
o
Location
Age , in
years B.P.
Description of sample
Significance
      RAY-GS-8
      (1-9831)
     RAY-GS-9
     (1-9852)
     RAY-GS-10
     (1-9972)
         Dansvllle quad.  , Red      <180
         School Road at Bradner
         Creek.  77°44'52" lat,
         42037'00" long.
         Sonyea quad.  , Pioneer  10,730 + 150
         Road at Erie-Lackawanna
         railroad.  77°49'00"
         lat, 42°41'15" long.
         Sonyea quad. , Erie-
         Lackawanna railroad
         at Keshequa Creek.
         77°49'39lf lat,
         42°41'50" long.
11,160 + 160
Log buried 1.8 m below
flood-plain surface (now
covered by dike).  Much
organic debris in logs
and gray sand

Lake clays with organic
debris below conspicuous
basal peat layer of 9.3 m.
Washed residue from 9.4
to 10.6 m depth in core

Wood and peat layer over-
lying lake clay section
(as in sample 9).  Dated
25-mm diameter wood frag-
ment with branches
                                           Shows  recent  marked  lateral
                                           migration  and(or)  aggrada-
                                           tion in  Canaseraga valley
Marks apparent end of
open lake and beginning
of shallow marsh-lake
environment in Canaseraga
Valley

Marks apparent end of
open lake and beginning
of shallow marsh-lake
environment in Canaseraga
valley
     1
     2
     3
Number in parenthesis is Teledyne analysis number.
Locations shown in figure 1.
Quadrangle; map published by U.S. Geological Survey, 1:24,000 scale.

-------
                                 REFERENCES

Dethier, B.  A.,  1966,  Precipitation  in  New  York State:   Ithaca,  N.Y.,
    Cornell  University Agriculture Experiment  Station,  Bulletin  1009,
    78  p.

Draper, N. R., and  Smith, H.,  1966,  Applied regression  analysis:   New
    York, John Wiley,  407 p.

Fairchild, H. L., 1926, The Dansville valley and  drainage history of
    western  New  York:  Rochester, N.Y.,  Proceedings  of  the Rochester
    Academy  of Sciences, v. 6,  p. 217-242.

        1928, Geologic  story of  the Genesee  valley and western New
    York:  Rochester, N.Y., H. L. Fairchild,  215  p.

Guy, H. P., 1969, Laboratory  theory and  methods for  sediment  analysis:
    U.S. Geological Survey, Techniques of Water-Resources  Investigations,
    book 5, chapter Cl, 58 p.

Guy, H. P., and Norman, V. W., 1970, Field methods for  measurement  of
    fluvial sediment:  U.S. Geological Survey, Techniques  of
    Water-Resources Investigations, book 3, chapter  C2,  59 p.

Hetling, L. J., Carlson, G. A., Bloomfield, J. A., Boulton, P.  W.,  and
    Rafferty, M. R., 1978, Summary pilot watershed report:  New York
    State Department of Environmental Conservation,  Bureau of Water
    Resources, 73 p.

Kammerer, J. C., and Hobba, W. A., Jr.,  1967, The geology  and availability
    of ground water in the Genesee River basin, New  York and Pennsylvania,
    ir± U.S. Army Corps of Engineers, Genesee River basin comprehensive
    study of water and related land resources:  Buffalo, N.Y.,  U.S. Array,
    Corps of Engineers, appendix I, 102 p.

Mansue, L. J., and Bauersfeld, W. R.   1983.  Part I:  Streamflow and sediment
    transport in the Genesee River basin, New York.  In Volume 4;   Streamflov
    and sediment transport, Final Report Genesee River Watershed. U.S. Envi-~
    rtontnental Protection Agency.

Mansue, L. J., Young, R.A., and Soren, J.  1983.  Part  II: Hydrogeologic
    influences on sediment transport patterns in the Genesee River  basin.
    In Volume IV:  Streamflow and sediment transport,  Final Report Genesee
    River Watershed.  U.S. Environmental Protection Agency.
                                 111-47

-------
Means, R. E-, and Parcher, J. V.,  1963,  Physical  properties  of soils:
    Merril Books, Inc., Columbus,  Ohio,  464  p.

Miller, N. G., 1973, Late glacial  and  post-glacial vegetation change in
    southwestern New York State:   New  York State  Museum and  Science Service,
    Bulletin 420, 102 p.
                                  111-48

-------
                                     TECHNICAL REPORT DATA
                             (Please read Inunctions on the rercrsi- before completing:
 1  REPORT NO
   EPA-905/9-91-005D
                                                              3. RECIPIENT'S ACCESSION-NO.
 4 TITLE ANDSUBTITLE
   Genesee River Watershed  Study
   Volume 4 - Special Studies  - U.S. Geological  Survey
                                                            8. REPORT DATE
                                                                 March 1978
                                                            6. PERFORMING ORGANIZATION CODE
 7. AUTHORIS)
   Lawrence  J. Mansue
   William R. Bauersfield
   Richard A. Young
                               Julian Soren
                               Todd S. Miller
                                                            B. PERFORMING ORGANIZATION REPORT NO.
 9. PERFORMING ORGANIZATION NAME AND ADDRESS
   New York State Department  of  Environmental Conservation
   Bureau of Technical  Services  and Research
   50  Wolf Road
   Albany, New York 12233
                                                            10. PROGRAM ELEMENT NO.
                                                              A42B2A
                                                            11. CONTRACT/GRANT NO.
                                                              R005144
 12. SPONSORING AGENCY NAME AND ADO~,IS_
  Great  Lakes National Program Office
  U.S. Environmental Protection Agency
  230  South Dearborn Street
  Chicago,  Illinois 60604
                                                            13. TYPE OF REPORT AND PERIOD COVERED
                                                              Final  -  1974-1978
                                                            14. SPONSORING AGENCY CODE
                                                              GLNPO/USEPA
 15. SUPPLEMENTARY NOTES
  Ralph  G.  Christensen, Grants  Officer
  Patricia  Longabucco, NY DEC Coord.
 16. ABSTRACT
    Part  I
                Streamflow and Sediment Transport in the Genesee River,  New York
    Part  II   -   Hydrogeologic  Influences on Sediment  Transport Patterns  in  the
                  Genesee River  Basin

    Part  III  -   Sources and Movement of Sediment in the  Canaseraga Creek Basin
                  near Dansville, New York
 7.
                                 KEY WORDS AND DOCUMENT ANALYSIS
                  DESCRIPTORS
                                               b.lDENTIFIERS/OPEN ENDED TERMS
                                                                           c. COS AT I Field/Group
  Sediment transport
  Water quality
  Stream flow
  Suspended sediment
  Precipitation
  Particle size
  Bedrock
                        Ground water
                        Land use
                        Minerology
 Document available to  public through
 National Technical Information Service
                                             19. SECURITY CLASS (ThisReport)
                                                None
21. NO. OF PAGES
      135
INTIS}
Springfield, VA   22161
                                               20. SECURITY CLASS (Thiipage)
                                                  None
                                                                         22. PRICE
EPA Form 2220-1 (9-73)
                                        111-49

-------