USDA
EPA
United States
Department of
Agriculture
Science & Education Admin
Cooperative Research
Washington DC 20250
CR 2
United States
Environmental Protection
Agency
Industrial Environmental Research
Laboratory
Cincinnati OH 45268
EPA 600 7-79-100
April 1979
Research and Development
Soil Genesis,
Hydrological
Properties, Root
Characteristics, and
Microbial Activity of
1- to 50-Year Old
Stripmine Spoils
Interagency
Energy/Environment
R&D Proaram
Report
-------
RESEARCH REPORTING SERIES
Research reports of the Office of Research and Development, U.S. Environmental
Protection Agency, have been grouped into nine series. These nine broad cate-
gories were established to facilitate further development and application of en-
vironmental technology. Elimination of traditional grouping was consciously
planned to foster technology transfer and a maximum interface in related fields.
The nine series are:
1. Environmental Health Effects Research
2. Environmental Protection Technology
3. Ecological Research
4. Environmental Monitoring
5. Socioeconomic Environmental Studies
6. Scientific and Technical Assessment Reports (STAR)
7. Interagency Energy-Environment Research and Development
8. "Special" Reports
9. Miscellaneous Reports
This report has been assigned to the INTERAGENCY ENERGY-ENVIRONMENT
RESEARCH AND DEVELOPMENT series. Reports in this series result from the
effort funded under the 17-agency Federal Energy/Environment Research and
Development Program. These studies relate to EPA's mission to protect the public
health and welfare from adverse effects of pollutants associated with energy sys-
tems. The goal of the Program is to assure the rapid development of domestic
energy supplies in an environmentally-compatible manner by providing the nec-
essary environmental data and control technology. Investigations include analy-
ses of the transport of energy-related pollutants and their health and ecological
effects; assessments of, and development of, control technologies for energy
systems; and integrated assessments of a wide range of energy-related environ-
mental issues.
This document is available to the public through the National Technical Informa-
tion Service, Springfield, Virginia 22161.
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EPA-600/7-79-100
April 1979
SOIL GENESIS, HYDROLOGICAL PROPERTIES, ROOT CHARACTERISTICS
AND MICROBIAL ACTIVITY OF 1-TO 50-YEAR-OLD STRIPMINE SPOILS
by
W. M. Schafer, G. A. Nielsen
D. J. Dollhopf, K. Temple
Montana Agricultural Experiment Station
Montana State University
Bozeman, Montana 59717
SEA-CR IAG No. D6-E762
Project Officer
Ronald D. Hill
Resource Extraction and Handling Division
Industrial Environmental Research Laboratory - Cincinnati
Cincinnati, Ohio 45268
This study was conducted in cooperation with the Science and Education
Administration, Cooperative Research, USDA, Washington, DC 20250.
INDUSTRIAL ENVIRONMENTAL RESEARCH LABORATORY
OFFICE OF RESEARCH AND DEVELOPMENT
U.S. ENVIRONMENTAL PROTECTION AGENCY
CINCINNATI, OHIO 45268
-------
DISCLAIMER
This report has been reviewed by the Industrial Environmental Research
Laboratory-Cincinnati, 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.
The views and conclusions contained in this report are those of the
authors and should not be interpreted as representing the official policies
or recommendations of the Science and Education Administration-Cooperative
Research, U. S. Department of Agriculture.
11
,
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FOREWORD
When energy and material resources are extracted, processed, converted,
and used, the related pollutional impacts on our enviornment and even on our
health often require that new and increasingly more efficient pollution
control methods be used. The Industrial Environmental Research Laboratory-
Cincinnati (IERL-Ci) assists in developing and demonstrating new and improved
methodologies that will meet these needs both efficiently and economically.
Strip-mining for coal drastically alters the landscape of a limited
number of acres in the Northern Great Plains each year. The cumulative effect
of mining over many years may significantly alter the soil resources of this
region. The Reclamation Research unit at Montana State University conducted
a two-year study funded by the SEA-CR (USDA) and USEPA to 1) evaluate
differences between native soils and soils on mined land and 2) study the
changes in soil properties through time that occur on minesoils.
Soil chemical and physical properties were measured in 15 soils; 5
natural soils, 5 minesoils nearly 50 years old, and 5 minesoils less than
10 years old. Soil water movement patterns, soil temperature changes, root
biomass, root uptake of radioactive phosphorus, and microbiological activity
of all soils were monitored.
Results of this study are discussed in the following pages. Projections
are made concerning soil development patterns, root growth rates, and micro-
biological activity as minesoils increase in age. Finally, recommendations
on ways to improve reclamation techniques and increase mine soil potential
are made. The results of this work should provide to the reclamation
specialist of a mining company or control agency additional methods to
establish good ground cover to minimize the environmental problem from surface
mining. For further information contact the Extraction Technology Branch of
the Resource Extraction and Handling Division.
Industrial
David G. Stephan
Director
Environmental Research
Cincinnati
Laboratory
iii
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ABSTRACT
A sequence of soils on mined land, minesoils, 1 to 50 years in age were
compared to many natural soils in southeastern Montana. The objective of
this study was to evaluate the potential impact of mining on soil resources
in the area, and to find what changes take place in minesoils through time
that may affect soil potential.
Young minesoils constructed before passage of the 1973 Montana Strip-
mine Reclamation Act were not as good as the best soils existing before
mining. Minesoils were better than some of the poorer soils on the natural
landscape, however. Minesoils currently being constructed in the Colstrip
vicinity (in 1977 and 1978) appear to be better than minesoils studied in
this report (constructed between 1970 and 1975). New minesoils (less than
10 years old) often support plant communities functionally more similar to
native plant communities than old minesoils (50 years old). Modern
reclamation techniques applied to suitable mines oils are more effective in
reestablishing productive grassland communities than 50 years of succession
on poor quality minesoils.
The natural processes which were active in the development of natural
soils were found to occur in 50-year-old minesoils. Only a small amount of
the change required to form the natural soils has taken place in minesoils,
however. Only 50 years were required for organic matter content, and soil
structure to reach levels common in natural soils in the top 5 cm of the
soils. Up to 500 years may be required for organic matter and soil
structure to reach equilibrium in deeper soil layers. As many as 10,000
years might be necessary for other soil properties such as calcium carbonate
distribution to resemble natural soils. Replacement of "topsoil" (material
salvaged from natural soils before mining) results in mine soils more similar
to natural soils. Because minesoils result from man-caused rather than
natural processes, it is probable they will always remain different from
natural soils. Although minesoils are different than natural soils, they are
not necessarily inferior. Minesoils constructed with high quality material in
stable slopes can be highly productive, perhaps surpassing the potential of
natural soils in some cases. The unique properties of minesoils will need to
be recognized and understood to properly manage mined areas.
Limited water is one of the most important factors governing plant growth
in the arid West. Minesoils should have a high water-holding capacity, and
high infiltration rate to maximize reclamation potential. Minesoils in this
study had rapid infiltration rates, which means that precipitation should
enter the soil rapidly so that little run-off occurs. Despite rapid infiltra-
tion rates, excessive run-off and erosion were common on poorly vegetated
mine soils during intense storms. Rapid vegetation establishment and other
iv
-------
erosion control measures are critical in protecting minesoils during the
first years after reclamation.
Patterns of water use differed in natural soils, old and new minesoils.
Plant communities on natural soils (mid- and short-grass prairie) used soil
water conservatively. Water use began slowly in April and May. reached a
peak in June, and continued at a slow rate through the summer. At the end of
the growing season, much of the plant available water still remained in the
root zone. Plant communities on old minesoils (half-shrubs and annual
grasses) used water rapidly from May through July, depleting nearly all the
available water in the root zone. Because of the complete use of water each
growing season, old minesoils have very little available water in a dry year
compared to natural soils which have a reserve of water remaining from the
previous growing season. Plant communities on new minesoils (introduced
perennial grasses) use water rapidly in early spring, but very slowly in the
summer. Total water use for the growing season is similar to that in natural
soils.
At least three to four years are required before root systems in mine-
soils resemble those in natural soils in weight and distribution. Roots
develop most rapidly near the soil surface, but more slowly below 50 em.
Roots penetrate as deeply as six feet in natural soils and minesoils.
Using a radioactive tracer, it was found that the only active roots late in
the growing season occur below 75 em. Less than 10% of all roots occur below
that depth.
Three to four years were required for microbiological activity to reach
the levels common in natural soils. More microorganisms were found in
natural soils than in minesoils at the 10 to 50 em depth. This could have
been due to the higher organic matter levels in natural soils at these
depths. Microbiological activity varied seasonally and was probably influ-
enced by soil temperature, nutrient availability, and by changes in the
amount of readily decomposable organic matter.
This final report is from SEA-CR project No. 684-15-4 entitled "Effects
of Species Root Distribution on Soil Biota-Genesis-Hydrological Characteristics~
v
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CONTENTS
Foreword.
Abstract.
Figures
Tables.
Acknowledgments
Hi
iv
xi
xv
xix
1.
2.
3.
4.
Introduction.
Conclusions
Recommendations
Literature Review
Soil Genesis
Soil Water Relations
Grassland Root Systems
Microbiological Activity
Study Area.
Location
Geology.
Soils.
Vegetation
Climate.
Land Use
Site Selection
Materials and Methods
Soil Characterization.
Water Movement
Root Biomass and Activity.
Microbiological Activity
Soil Development and Characterization
Colstrip History
Soil Morphology.
Carbon and Nitrogen Profiles
Phosphorus Fractions
Mobile Soil Components
Soluble salts
Calcium carbonate
Trace Elements
Clay Mineralogy.
Fabric-related Properties.
Clay.
Soil structure.
Bulk density.
Rock fragments.
Orphan spoils
1
3
7
12
12
14
17
20
22
22
22
26
30
30
31
32
35
35
36
38
41
43
43
46
47
48
51
51
53
57
65
66
66
66
68
69
73
5.
6.
7.
vii
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10.
8.
Water Relations.
Infiltration.
Water Flow Patterns
Soil Water Potential.
Soil Temperature.
Root Characteristics
Root Biomass.
Radioactive Phosphorus Uptake
Microbiological Activity
9.
Literature Cited
Appendices
A.
Soil Characterization.
Pedon descriptions and laboratory
Water Relations.
Infiltration.
Volumetric soil water content
Soil temperature.
Root Activity.
Plant activity index equation
Plant radioactivity field counts.
Plant activity index.
B.
C.
viii
80
80
81
103
103
105
105
106
116
125
136
136
data. 136
181
181
184
187
188
188
190
209
-------
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure 10.
Figure 11.
Figure 12.
Figure 13.
Figure 14.
Figure 15.
FIGURES
1.
Map showing Co1strip study area location and LANDSAT-1
image of the region (NASA). .. . . . . . . . . . . . . . . .
2.
Typical landscape in the Co1strip area.
.......
3.
Stratigraphic section in the Co1strip area
......
4.
Co1strip region soils map showing dominant soil
associations. . . . . .. ........
......
5.
Representative slope profile and soil series which develop
on various parent materials at each geomorphic position
in the Co1strip, Montana area. . . . . . . . . . . . . . . .
6.
Location of 15 research sites near Co1strip, Montana. The
site names represent either the soil series if natural
soils, or date of last disturbance of mine soils. . . . . .
7.
Arrangement of research exc10sures .
............
8.
Anti-coincidence detector. . . . .
........
.....
9.
Schematic diagram of circuitry in anti-coincidence
detec tor. . . . . . . . . . .
Foley Bros. mining operation at Co1strip in 1928 . .
. . . .
(Left) spoil platform being deposited with a side-dumping
Mack truck in 1929, (Right) material for 1929-10 site was
stripped from the right side of photo and dumped on the
Ie ft. . . . . . . . . . . . . . . . . . . . . . . . .
1931 Aerial photo taken of 1928 spoils showing vegetation. .
Range in organic carbon content of natural soils and
minesoils . . . . . . . . . . . . . . . . . .
. . . .
Organic carbon accumulation through time showing
fraction in litter. . . . . . . . . . . . . . .
Range in electrical conductivity in natural soils and
minesoils. . . . . .. ...............
. . .
ix
Page
23
24
25
27
29
33
35
39
40
43
44
45
47
49
52
-------
Figure 16.
Figure 17.
Figure 18.
Figure 19.
Figure 20.
Figure 21.
Figure 22.
Figure 23.
Figure 24.
Figure 25.
Figure 26.
Figure 27.
Figure 28.
Figure 29.
Figure 30.
Figure 31.
Figure 32.
Figure 33.
Figure 34.
Range in calcium carbonate content in natural soils and
minesoils. . . . . . . . . . . . . . . . . . . . . . . . . .
Thin section of soil pore at 100 cm in old minesoil
showing carbonate enrichment. . . . . . . . . .
. . . .
Thin section of sandstone fragment (lower portion of photo)
in old minesoil.. Fragment has large CaC03 crystals in
interior but small recrystallized CaC03 around rim. . . . . .
Range in pH for natural soils and minesoils . . . . .
. . . .
Distribution of DTPA-extractable Zn, Fe, Mn, and Cu in
natural soils and minesoils . . . . . . . . . . . . . .
. . .
Bands of iron staining parallel the low chroma sandstone
fragment in the center of the picture. . . . . . . . . . . .
Thin section of siltstone fragment showing manganese bands
(mangans) paralleling fractures. . . . . . . . . . . . . . .
Distribution of DTPA-extractable Pb, Ni, and Cd in
natural soils and minesoils. . . . . . . . . . . . . .
. . .
Coal fragment showing bands.of iron-staining paralleling
fragment. White material around coal is gypsum. . . . . . .
Range in clay content for natural soils and minesoils
. . . .
Oriented clay (argillans) around sand grains of Boxwell B
horizon. . . . . . . . . . . . . . . . . . .. ....
Range in kinds of structure in natural soils and minesoils.. .
Range in structure grade in natural soils and minesoils . . .
Granular structure in old mine soils is associated with
the root systems of perennial grasses. . . . . . . . . .
Range in bulk density for natural soils and mines oils . . . .
Scrapers (left) and bulldozers (right) create minesoils
with different bulk densities. . . . . . . .. ....
A single shale fragment is shown to weather more quickly
near the soil surface in this four-year-old minesoil . . . .
Rock fragment content of mine soils varying in age. .
. . . .
Photo of 1928 minesoi1 showing that rock fragments have
x
Page
55
56
57
-58
59
61
62
63
64
67
68
69
70
. .
71
72
73
74
75
-------
Figure 35.
Figure 36.
Figure 37.
Figure 38.
Figure 39.
Figure 40.
Figure 41.
Figure 42.
Figure 43.
Figure 44.
Figure 45.
Page
weathered in the upper 20 cm but are common below that depth.
76
Thin sections taken within unweathered (above) and weathered
(below) sandstone fragments. CaC03 occurs in discrete grains
in unweathered fragments but is dispersed in the weathered
state. . .
. . . .
77
.....................
Vegetated, non-vegetated, and crusted areas occur in close
proximity on orphan spoils. . . . . . . . . . . . . .
78
Average monthly precipitation is shown in comparison to
1976 and 1977 totals. . . . . . . . . . . . . . . . .
82
Profile water content (cm in upper 150 cm) is shown as a
percentage of the recharged content in June, 1976. The
line at 50% represents the approximate wilting point.
84
Seasonal water content, bulk density, and root biomass for
the Chinook-l soil. . . . . . . . . . . . . . . .. ....
85
Seasonal water content, bulk density, and root biomass for
the Boxwe11-2 soil. . . . . . . . . . . . . . . . . . . . .
86
Seasonal water content, bulk density, and root biomass for
the 1948-3 soil. . . . . . . . . . . . . . . . . . . .
87
Seasonal water content, bulk density, and root biomass for
the Ethridge-4 soil. . . . . . . . . . . . . . . . . . . . .
88
Seasonal water content, bulk density, and root biomass for
the 1928-5 soil. . . . . . . . . . . . . . . . . . . .
89
Seasonal water content, bulk density, and root biomass for
the Riedel-6 soil. . . . . . . . . . . . . . . . . . .
90
Seasonal water content, bulk density, and root biomass for
the 1928-7 soil. . . . . . . . . . . . . . . . . . . .
91
Figure 46. Seasonal water content, bulk density, and root biomass for
the Chinook-8 soil. . . . . . . . . . . . . . . . . . . . . 92
Figure 47. Seasonal water content, bulk density, and root biomass for
the 1928-9 soil. . . . . . . . . . . . . . . . . . . . . . . 93
Figure 48. Seasonal water content, bulk density, and root biomass for
the 1929-10 soil . . . . . . . . . . . . . . . . . . . . . . 94
Figure 49. Seasonal water content, bulk density, and root biomass for
the 1975-11 soil . . . . . . . . . . . . . . . . . . . . . . 95
xi
-------
Page
Figure 50. Seasonal water content, bulk density, and root biomass for
the 1973-12 soil. . . . . . . . . . . . . . . . . . . . . . 96
Figure 51. Seasonal water content, bulk dens ity, and root biomass for
the 1972-13 soil. . . . . . . . . . . . . . . . . . . . . . 97
Figure 52. Seasonal water content, bulk density, and root biomass for
the 1969-14 soil. . . . . . . . . . . . . . . . . . . . . . !l8
Figure 53. Seasonal water content, bulk density, and root biomass for
the 1970-15 soil. . . . . . . . . . . . . . . . . . . . . . 99
Figure 54. Radioautographs of a grass (needle-and-thread) and a half-
shrub (broom snakeweed) showing p32 accumulation in the
meristematic regions. . . . . . . . . . . . . . . . . . . . 107
Figure 55. Average plant activity index for various vegetative types
through the 1977- growing season . . . . . . . . . . . . . . 112
Figure 56. Average plant activity index for uptake from several soil
depths through the 1977 growing season. . . . . . . . . . . 113
Figure
57.
Plant activity index of several species at the Chinook-l
site is shown in relation to seasonal changes in soil
temperature and water content at several depths
115
Figure
58.
ATP activity in natural soils, August, 1976 .
. . . .
117
Figure
59.
ATP activity in old minesoils, August, 1976.
. . . .
118
Figure 60. ATP activity in new mines oils , August, 1976. . . . . 119
Figure 61. ATP activity in selected soils, June, 1977. . . . . . 121
Figure 62. ATP activity in selected so ils, October, 1977 . . . . . . . 122
Figure A-l. Photograph of Chinook-l soil profile. . . . . . . . . . . . 138
Figure A-2. Photograph of Boxwel1-2 soil profile. . . . . . . . . . . . 141
Figure A-3.
Photograph of 1948-3 soil profile. .
......
.....
144
Figure A-4.
Photograph of Ethridge-4 soil profile.
..........
147
Figure A-5.
Photograph of 1928-5 soil profile. .
.....
150
Figure A-6.
Photograph of Riedel-6 soil profile. .
. . . .
153
Figure A-7.
Photograph of 1928-7 s011 profile.
. . . .
.....
156
xii
-------
Page
Figure A-8. Photograph of Chinook-8 soil profile 159
Figure A-9. Photograph of 1928-9 soil profile 162
Figure A-10. Photograph of 1929-10 soil profile 165
Figure A-ll. Photograph of 1975-11 soil profile 168
Figure A-12. Photograph of 1973-12 soil profile 171
Figure A-13. Photograph of 1972-13 soil profile 174
Figure A-14. Photograph of 1969-14 soil profile 177
Figure A-15. Photograph of 1970-15 soil profile 180
Figure B-l. Infiltration vs time measured in undisturbed soils at the
Colstrip study area in August, 1976 181
Figure B-2. Infiltration vs time measured in old spoils at the Colstrip
study area in August, 1976 182
Figure B-3. Infiltration vs time measured in new spoils at the
Colstrip study area in August, 1976 183
Figure C-l. Plant radioactivities measured in situ on undisturbed
soils at the Colstrip study area in 1976 190
Figure C-2. Plant Radioactivities measured in situ on old spoils
at the Colstrip study area in 1976 191
Figure C-3. Plant radioactivities measured in situ on new spoils
at the Colstrip study area in 1976 192
Figure C-4. In situ plant radioactivities on Chinook-1 undisturbed
soil at Colstrip study area - replication 1, 1977 193
Figure C-5. In situ plant radioactivities on Chinook-1 undisturbed
soil at Colstrip study area - replication 2, 1977 194
Figure C-6. In situ plant radioactivities on Chinook-1 undisturbed
soil at Colstrip study area - replication 3, 1977 195
Figure C-7. In situ plant radioactivities on 1929-10 spoil at
Colstrip study area - replication 1, 1977 196
Figure C-8. In situ plant radioactivities on 1929-10 spoil at
Colstrip study area - replication 2, 1977 197
xiii
-------
Figure
C-9.
Figure C-10.
Figure C-ll.
Figure C-12.
Page
In situ plant radioactivities on 1929-10 spoil at
Colstrip study area - replication 3, 1977. . . . . . . . .
198
In situ plant radioactivities on 1970-15 spoil at
Colstrip study area - replication 1, 1977. . . . . . . . .
In situ plant radioactivities on 1970-15 spoil at
Colstrip study area - replication 2, 1977. . . . .
In situ plant radioactivities on 1970-15 spoil at
Colstrip study area - replication 3, 1977. . . . .
199
. . . . 200
. . . . 201
Figure C-13. In situ plant radioactivities on Boxwell-2 undisturbed
so il at Colstrip study area - replication 1, 1977. . . . . 202
Figure C-14. In si tu plant radioactivities on Chinook-8 undisturbed
soil at Colstrip study area - replication 1, 1977. . . . . 2113
Figure C-15.
Figure C-16.
Figure C-17.
Figure C-18.
Figure C-19.
In situ plant radioactivities on 1948-3 spoil at
Colstrip study area - replication 1, 1977. . . . . . . . .
In situ plant radioactivities on 1969-14 spoil at
Colstrip study area - replication 1, 1977. . . . .
In situ plant radioactivities on 1972-13 spoil at
Colstrip study area - replication 1, 1977. . . . .
In situ plant radioactivities on 1973-12 spoil at
Colstrip study area - replication 1, 1977. . . . .
In situ plant radioactivities on 1975-11 spoil at
Colstrip study area - replication 1, 1977. . . . .
xiv
204
. . . . 205
. . . . 206
. . . . 207
. . . . 208
-------
Table
Table
Table
Table
Table
Table
Table
Table
Table
Table 10.
Table 11.
Table 12.
TABLES
1.
Annual precipitation at Colstrip, Montana for the years
1928-1977. . . . . . . . . . . . . . . . . . . .
. . . .
2.
Description of origin, characteristics, and management
of research sites. Sites were chosen to represent the
diversity of characteristics as well as typical aspects
of mine soils and undisturbed soils in the Colstrip area
3.
Abundance of roots by number and size. . .
.....
.....
4.
Composition of minesoils based on 3 point counts of
100 counts each at 50 cm depth. Several different types
of rock fragments occur in mine soils. . . . . . . . . .
5.
Organic carbon accumulated at various depths in soils at
Colstrip. Natural soils have less carbon in litter and
a smaller C/N ratio than minesoils. . . . . . . . . . .
6.
Fractions of inorganic and organic phosphorus in a typical
natural soil, old minesoil, and new minesoil . . . . .
7.
Partial ionic composition of a saturation extract is shown
from two depths for ea~h soil. Plant nutrients such as K+
are concentrated in surface horizons which indicates
nutrient cycling has caused the surface salt accumulation
observed in these soils. . . . . . . . . . . . . . . . .
8.
Years required for carbonate removal to occur in five
soils near Colstrip. . . . . . . . . . . . . . .
. . . .
9.
Clay mineral abundance in the clay fraction of natural
soils andminesoils, at Colstrip, Montana. . . . . . .
. . . .
Selected soil analyses from vegetated, non-vegetated,
and non-vegetated, crusted orphan spoils in the Colstrip,
Man tana area. .. ......................
Infiltration rate after 30 minutes on natural soils and
minesoils of the Colstrip, Montana area. . . . . . . . .
Correlation between root biomass and water use from 4/4/77 to
6/15/77 at three depths in natural soils; old, and new
xv
Page
31
34
38
46
48
50
54
56
65
79
. . 81
-------
Table 13.
Table 14.
Table 15.
Table 16.
Table 17.
Table 18.
Table 19.
Table 20.
Table 21.
Table A-I
Table A-2
Table A-3
Table A-4
Table A-5
Table A-6
Table A-7
minesoils.
. . . . . . .
. . . . . . .
.......
. . . .
Vegetative production in 1976 and 1977 was predicted from
the amount of stored soil water depleted from the upper
150 cm, and summer precipitation using multiple linear
regression. . . . . . . . . . . . . . . . . . . .
Soil temperatures at 50 cm in spring, summer, fall, and
winter were graphically inferred from a plot of all soil
temperature data. Mean annual soil temperature was
calculated from the mean of seasonal temperatures. . . . .
Page
. 101
. . . 102
. . 104
Root biomass, the proportion of roots in surface horizons,
and the fraction of roots in various size classes is shown
for natural soils and minesoils. . . . . . .. ....... 1()5
Summary of plant activity index (PAl) values for various
vegetation types on Colstrip soils during 1976 and 1977. . . . 107
Summary of plant activity index (PAl) values representing
p32 uptake from various soil depths of Colstrip soils
during 1976 and 1977. . . . . . . . . .. .....
Maximum observed rooting depths using p32 tracer in
Colstrip soils. . . . .. ...........
32
Analysis of variance for P uptake showing sources of
variation for the 1976 growing season. . . . . . . . . . .
. . 108
. . . . 109
. . 110
Average plant activity index (PAl) values from all species
and all soil depths are shown for the 1976 and 1977
growing seasons on Colstrip soils. . . . . . . . . . . . . . . 110
ATP activity of rhizoplane, rhizosphere, and free soil for
selected plants from several research sites. . . . . .
Pedon Description of Chinook-l soil. .
........
Laboratory analyses of Chinook-l soil.
. . . .
Pedon description of Boxwell-2 soil. . .
.....
. . . .
Laboratory analyses of Boxwell-2 soil.
........
Pedon description of 1948-3 soil.
.........
. . . .
Laboratory analyses of 1948-3 soil. .
.......
Pedon description of Ethridge-4 soil. .
. . . .
.....
xvi
. 123
. 136
. , 137
. . 139
. . . . 140
. 142
. . 143
. . 145
-------
Table
A-8.
Table
A-9.
Table A-10.
Table A-H.
Table A-12.
Table A-13.
Table A-14.
Table A-15.
Table A-16.
Table A-17.
Table A-18.
Table A-19.
Table A-20.
Table A-2l.
Table A-22.
Table A-23.
Page
Laboratory analyses of Ethridge-4 soil. .
......
146
Pedon description of 1928-5 soil. .
............
148
Laboratory analyses of 1928-5 soil. .
......
.....
149
Pedon description of Riedel-6 soil.
......
151
Laboratory analyses of Riedel-6 soil. .
. . . .
152
Pedon description of 1928-7 soil. .
.....
. . . .
154
Laboratory analyses of 1928-7 soil. .
.....
155
Pedon description of Chinook-8 soil.
......
.....
157
Laboratory analyses of Chinook-8 soil.
..........
158
Pedon description of 1928-9 soil. . .
.....
160
Laboratory analyses of 1928-9 soi1. . .
..........
161
Pedon description of 1929-10 soil. . .
.......
163
Laboratory analyses of 1929-10 soil
......
164
Pedon description of 1975-11 soil. . .
. . . .
166
Laboratory analyses of 1975-11 soil.
.....
167
......
Pedon description of 1973-12 soil. . .
. . . .
169
Table A-24. Laboratory analyses of 1973-12 soil . . . . . . . . . . . . 170
Table A-25. Pedon description of 1972-13 soil . . . . . . . . . . . . . 172
Table A-26. Laboratory analyses of 1972-13 soil . . . . . . 173
Table A-27. Pedon description of 1969-14 soil . . . . . . . . . . 175
Table A-28. Laboratory analyses of 1969-14 soil . . . . . . . . . 116
Table A-29. Pedon description of 1970-15 soil . . . . . . . . . . . . . 178
Table A-30. Laboratory analyses of 1970-15 soil . . . . . . . . . 179
Table
B-l.
Table
B-2.
Volumetric soil water content (%) at selected depths in
natural soils near Colstrip, Montana. . . . . . . . . . . .
184
Volumetric soil water content (%) at selected depths in
xvii
-------
Page
old "minesoils near Colstrip, Montana. . . . .
......
. 185
Table
B-3.
Volumetric soil water content (%) at selected depths in
new minesoils near Colstrip, Montana. . . . . . .
. . 186
Table
B-4.
80il temperatures (OC) for undisturbed soils and
minespoils at Colstrip study area. . . . . . . . . . .
. . . 187
Table C-l. Plant activity index (PAl) values obtained from native
range soils near Colstrip, Montana . . . . . . . . . . . . . 209
Table C-2. Plant activity index (PAl) values obtained from old mine
soils near Colstrip, Montana. . . . . . . . . . . . . . . . 210
Table C-3. Plant activity index (PAl) values obatined from new mine
soils near Colstrip, Montana. . . . . . . . . . . . . . . . 211
xviii
-------
ACKNOWLEDGMENTS
The authors wish to express their thanks to the many individuals and
institutions who made this work possible. The Western Energy Co. is due
thanks for approving the study on newly reclaimed areas, and for lending
equipment and personnel support during various phases of the study. The
USDA Soil Conservation Service (SCS) participated extensively in the study.
The SCS field office in Forsyth, Montana as well as the Montana State office
aided in site selection, soil description, and sample collection. Dr. W.D.
Nettleton and others from the SCS Soil Survey Laboratory in Lincoln, Nebraska
assisted in sample collection and provided laboratory analyses of soil
samples.
Mr. John W~att carried out much of the field research related to water
movement and p3 uptake in conjunction with graduate studies at Montana State
University. Dr. Reid Howald, the radiological safety officer, provided
assistance in the handling and licensing requirements for p32 and neutron
probe use. Dr. John Amend of the Chemistry department designed the anti-
coincidence Geiger-Muller detector used for measuring p32 uptake.
Anne Camper, Debra Hansen, and Peggy Schaplow of the Microbiology
department performed parts of the field and laboratory work involved with
measuring ATP activity. Dr. Frank Munshower and Mr. Dennis Neuman performed
selected soil analyses including trace element chemistry. Many thanks are
due numerous other staff members of the Reclamation Research Unit and Plant
and Soil Science department for helpful suggestions and review comments.
John A. Asleson served as Project Director for
Experiment Station, and Eilif V. Miller coordinated
and Education Administration, Cooperative Research,
the Montana Agricultural
the effort for the Science
USDA.
This report was approved by the Montana Agricultural Experiment Station
for publication.
xix
-------
SECTION 1
INTRODUCTION
Strippable coal deposits underlay 2.6 million acres of land in the
Northern Great Plains. If energy demands grow as expected, approximately
100,000 acres will be mined in this region by the year 2000. Loss of pro-
ductivity from this land area would have a small impact on region-wide
agricultural production (NGPRP, 1975), however, impacts on local economy and
on long-term productivity would be more significant. This loss of produc-
tivity coupled with public environmental concern makes rehabilitation of
mined land a key issue in energy resource development.
The coal extraction process drastically alters the physical and biologi-
cal nature (ecosystem) of a mine area. Rehabilitation of mined land is
impossible without an understanding of geologic, hydrologic, biologic and
edaphic processes operating in unmined landscapes. In addition, the charac-
teristics of mine spoil must be well understood. Rehabilitation procedures
are also dependent on the intended post mining use of mined land. Dominant
land uses in the Northern Great Plains include 1) pasture and rangeland (69%),
2) dryland agriculture (25%), 3) forest and woodland (4%), 4) urban (1%), and
5) irrigated cropland (1%) (NGPRP, 1975). The potential may exist, through
mining, of creating land resources designed to satisfy local needs such as
stock-water impoundments, irrigated agriculture, quality pastureland, or
urban development. Before these goals can be achieved, however, more
knowledge about pre- and post-mine landscapes are needed.
A typical unmined landscape in the Northern Great Plains consists of 20
to 150 feet of weakly cemented sandstone, siltstone, and shale in varying
amounts overlying a thick coal seam; a moderately developed soil immediately
below the land surface formed during a 10,000 year period; and a plant
community which has developed in response to the climate, soil, and grazing
history at that location. After mining, this same area will consist of a
rolling topography offractured rock mixed from all segments of the overburden
without vegetation or established stream channels. Material salvaged from
soil horizons before mining is respread to speed soil development. The mined
landscape has been permanently altered. Successful rehabilitation of this
land depends on our ability to understand differences between mined and
unmined land and to isolate problems associated with mined areas.
In response to the need to better understand mined land, and in particu-
lar, soils on mined land, a study was initiated at Montana State University
to evaluate soil development on mine spoil. Soil water flow patterns, root
growth and development, and soil physical, chemical and microbiological
properties were investigated on minesoils 1 to 50 years in age, and on
1
-------
undisturbed soils. Differences between minesoils and undisturbed soils,
and changes in minesoils through time were evaluated.
2
-------
SECTION 2
CONCLUSIONS
Soil Genesis
1.
Processes which have formed natural soils in the Colstrip area are also
occurring in minesoils. Only a small part of the change that created
natural soils has occurred in 50-year-old minesoils.
2.
The genetic youth of minesoils does not severely limit reclamation po-
tential. In some cases the potential of minesoils is higher than for
natural soils.
3.
Some soil properties change rapidly in minesoils and may reach equilibri-
um in 200 to 400 years. These include organic matter content, pH, and
soil structure. Other properties such as CaC03 distribution may require
as much as 10,000 years to resemble native soils. Because of their
unique origin, minesoils will probably always remain different than un-
disturbed soils in some ways.
4.
Minesoils have wider C/N ratios than natural soils, and a large fraction
of the total carbon and nitrogen in minesoils is in the form of plant
litter. Organic carbon content in these soils increases rapidly near the
surface but very slowly below 10 cm.
5.
The amount and distribution with depth of extractable Fe, Mn, Cu, Zn, Ni,
Cd, and Pb was similar in old minesoils and natural soils. Differences
in concentrations with depth were related to organic carbon content, pH,
clay content, and other soil properties. The extractable trace element
levels in new spoils were closely related to the characteristics and
origin of the overburden fragments making up the soil parent material.
Levels of most elements were higher on new minesoils but did not for the
most part exceed potentially toxic levels (Montana Department of State
Lands, 1977). Evidence of movement and changes in the oxidation of Mn and
Fe was observed in thin sections of new minesoils.
6.
Bulk density of minesoils was closely related to the machinery used in
deposition of the spoils. Side-dumping haul trucks used in construction
of old spoils; and bulldozers, and draglines resulted in uncompacted mine
soils. Use of scrapers, however, often resulted in compacted zones with bulk
density of 1.7 to 1.9 g/cm3. Few compacted layers were found within
20 cm of the soil surface perhaps due to freezing and thawing or wetting
and drying of soils.
7.
Some orphan spoils (ungraded ridges left from mining during 1930-1940)
were found to have extremely acid surface horizons. Coal fragments with
abundant pyrite underlay these acid spots. Development of low pH under
3
-------
the semiarid climate typical of Colstrip indicated that high precipitation
is not a prerequisite for acid-production. It is a result instead of the
balance of acid-producing (pyrite) and neutralizing (CaC03) materials in
the overburden. Nearly all overburden material in the western states
contains a surplus of neutralizing materials.
Water Relations
1.
Infiltration rates were moderately rapid on both undisturbed soils and
minesoils. Despite the high infiltration rates, erosion was still a
major problem on new minesoils. Rapid establishment of vegetation and
use of erosion control is critical even on minesoils with moderately
rapid infiltration.
2.
The percentage of water held in soils in early spring after recharge was
determined largely by the water-holding capacity of the soil. The pat-
tern of water use through the growing season was influenced by the plant
community on each soil. Communities on new minesoils consisting primarily
of introduced perennial grasses used water rapidly in early spring in
the upper 50 cm. Shrub-dominated communities on old minesoils used
nearly all available water in the top 200 cm. Native plant communities
used water conservatively but water use continued through most of the
growing season unlike introduced plants on new minesoils.
3.
Introduced plants on minesoils had the highest water use efficiency of
stored soil water, but summer precipitation was not used to a significant
extent. Native plant communities utilized summer precipitation but not
as efficiently as they used stored soil water.
4.
The sparse vegetation on young minesoils did not use much of the water
available in the soil. As a result, drainage below the root zone would
be expected to be greater from newly planted minesoils than from mine-
soils with well-established vegetation. Drainage of water from new mine-
soils may affect the quantity and quality of acquifers developing in
spoils.
5.
The water use pattern in minesoils with 4-to 6-year-old reclaimed plant
communities was remarkably similar to natural soils. Proper reclamation
techniques on suitable soil materials were more effective in reestablish-
ing plant communities functionally similar to native communities than 50
years of succession on less suitable soils.
6.
The soil moisture regime of all soils was ustic (subhurnid) bordering on
aridic. Soils would qualify for aridic subgroups of Mollisols, Entisols,
and Inceptisols. The soil temperature regime of all soils was mesic but
bordered on frigid. New minesoils were cooler than natural soils while
old minesoils were warmer.
Root Activity
1.
Soil temperature and water potential affect root activity but genetic
4
-------
differences in plants make some species better able to withstand extremes
of the soil environment.
2.
Nearly twice as many roots occur in old minesoils as in natural soils and
new minesoils. The roots in old minesoils are larger in size and a
larger fraction occurs below 25 cm than in other soils. These differences
in root characteristics reflect the deep-rooted shrub-dominated plant
community on old minesoils. Deep-rooted plants have the advantage of
increased drought tolerance by having a larger available reservoir of
water as a result of the deeper root zone. However, less water per unit
weight of roots is obtained by deep-rooted plants. Therefore deep roots
form at the expense of above ground productivity since a larger fraction
of photosynthate must be utilized by the root system.
3.
Many perennial grasses, forbs, and shrubs have roots at least as deep as
150 cm in old and new minesoils;and in natural soils.
4.
Roots below 50 cm comprise only a small fraction of the total root biomass
but are extremely important in providing water and nutrients to plants
late in the growing season.
5.
Introduced perennial grasses common on new minesoils have higher root
activity early in the growing season but plants also senesce earlier than
native vegetation. Few species are active on minesoils after June while
some plants remain active on natural soils at least through late July.
6.
Four to six years were required for root systems to develop on new mine-
soils that are similar in biomass and distribution to root systems of
native plant communities. Roots develop more rapidly at shallow depths
than at deeper depths.
7.
Root activity differed in 1976 and 1977.
different in these two years. Roots were
which had a wet spring. It appears that
environmental factors is dynamic so that
yearly climatic fluctuations.
Rainfall distribution was also
active at deeper depths in 1976
the response of root systems to
growth patterns can adjust to
Microbiological Activity
1.
Microbial activity, as measured by ATP levels at three points in the
growing season, was within normal limits for range soils in the vicinity.
This indicates a satisfactory level of microbial activity had been
attained in all minesoils sampled. However, the 1948-3 site appeared to
be lower in microbial activity than any of the others.
2.
Seasonal variation in the ATP concentration with depth is apparent from
the similarity between August and October ATP profiles when compared to
June samples. Nevertheless, maximum ATP was high at most sites at a
shallow depth. One exception to this generalization was the 1975-11 site
which was sampled only once but had a lower-than-average ATP, with espe-
cially low surface and near-surface values. Coupled with the abnormal
ATP depth profile of the site, this may reflect the youth of this minesoil.
5
-------
Of all the sites sampled, the 1975-11 site showed the least resemblance
to a normally-developed soil in the ATP picture. The oldest sites,
deposited from 1920 to 1930 and with rev~getation by voluntary seeding,
had fairly consistent ATP profiles regardless of the type of plant cover
which had developed.
3. ATP measurements indicate that all minesoils progressed within several
years to a condition where microbial activity was at a level normal for
the climate and vegetation of the area. Only two sites, one prepared in
1975 and sampled in 1976, and the other the 1948-3 site, failed to show
this pattern of development of microbial activity. Of all sites, the
1972-13 site which has received perhaps more intensive management than
most reclaimed sites, was the highest in microbial activity as measured
by ATP.
6
-------
SECTION 3
RECOMMENDATIONS
General
1.
Based on an in-depth study of soils on mined land and on natural land-
scapes, several recommendations can be made regarding suitable tech-
niques for reconstructing minesoils. These suggestions will not apply
to all parts of the Northern Great Plains because of the unique condi-
tions encountered at each mine.
Material and Deposition: Best available material in a mine area should
be used in rebuilding minesoils. In the Colstrip area, the A, B, and
part of the C horizons of natural soils are consistently superior in
quality to much of the overburden. However, some of the sandy-loam and
loam-textured overburden low in salts is as good as the C horizons.
With the aid of detailed soil surveys, it is suggested that 50 to 150
cm of the best quality soils be salvaged before mining and respread on
the recontoured spoil surface at an average depth of 75 cm. When pos-
sible, cover-soil should be respread immediately after collection to
avoid the need for stockpiling which may degrade soil quality. The
upper layers of minesoils should consist of A horizon material because
it contains more organic matter, will develop soil structure more
rapidly, and contains native seed and plant parts that will aid revege-
tation. Cover-soil should be underlain by sandy loam or loam spoils
with low EC and few siltstone fragments. Large differences in texture
between spoils and cover-soil must be avoided so water and, roots can
penetrate the cover-soil/spoil interface. Use of scrapers to deposit
spoils should be avoided where possible to prevent stratifications and
compaction in the upper 200 cm of minesoils. When scrapers must be
used, deposited material should be chiseled to reduce compaction and
promote mixing of contrasting layers.
Landscape Design: Fine-sand-sized material, which is dominant in Col-
strip soils and overburden is easily eroded by running water. Long
slopes with more than 8-12% slope should be avoided, unless strict
conservation measures are implemented. Geomorphic principles should be
used to design a stable slope form suitable for unconsolidated spoil
material. Stable drainages with a coarser-textured channel bed should
be constructed in a drainage network complimentary to the slopes,vege-
tat ion and watersheds created on the mined area. Long, planar slopes
typical of reduced highwalls are particularly susceptible to rill and
gully development and must be avoided. Convex slopes are common on
some spoils, but are less stable than the concave slopes which develop
on similar materials in the natural landscapes.
7
-------
Management: Proper management of mined land is a key to successful
reclamation. Since 3 to 4 years are required for root systems to
develop, careful management including fertilization and irrigation
may be desirable initially. After this establishment period, the
degree of management required will depend on the type of vegetative
cover. Use of introduced species will require more careful manage-
ment and more frequent inputs than native plant communities. Heavy
fertilization of introduced species results in high productivity.
but also causes high rates of water use. As a result, little
plant-available water will remain in heavily fertilized minesoils
at the end of an average growing season. This is unlike natural
soils which have a small reserve of water at the end of an average
year. Consequently, these minesoils will be more adversely affected
by a dry year, resulting in more erratic vegetative productivity.
Another consequence of heavy fertilization is rapid litter accumu-
lation. Enough litter accumulates on 3- to 6-year-old minesoils
to retard productivity despite nearly equal amounts of microorgan-
isms in minesoils and natural soils. Controlled burning or grazing
properly used, are two techniques that may be employed to prevent
litter accumulation. Establishment of native plant communities
of a diverse nature with only moderate initial fertilization will
result in more stable ecosystems with fewer management needs.
Many years may be required for this goal to be reached succession-
ally, however. Minesoils will never be identical to natural soils.
They will often have a lower potential than the best natural soils
before mining but if properly constructed are likely to be superior
to many natural soils. Minesoils can support viable land uses if
quality soil materials are utilized, minesoils are properly con-
structed, slopes are geomorphically stable, and reclaimed areas
are suitably managed.
2.
The number of years required for mined land to be adequately restored
depends on the final land use. When the final use is livestock
grazing as in the Colstrip area, the time required is determined
by the type of vegetative cover desired: introduced species or
native. When introduced species are used, 3 to 4 years are requir-
ed for root systems to develop and for perennial plants to become
established. If periodic fertilization, controlled grazing, burn-
ing, and perhaps irrigation are acceptable as required management
tools, then mined areas may be "restored" at Colstrip in as little
as five years. If these management requirements are not acceptable,
and a self-sustaining, diverse cover of native species is desired,
then up to 20 years or more may be required. New techniques for
establishing native species may shorten this time period. To
speed nutrient cycling of nitrogen, phosphorus, and some other
essential nutrients, techniques to rapidly increase organic matter
content should be applied. These techniques include use of cover-
soil high in organic matter, incorporation of sludge or other or-
ganic wastes, or repeated cropping of vigorous annual grains which
produce extensive root systems.
3.
Development of a classification for minesoils would group minesoils
8
-------
with similar management needs, properties, and limitations into defined
units. In this way, research results on particular kinds of minesoils
could be extended or adapted to minesoils in other areas. The current
system used in the U.S. for classifying soils is the Seventh Approxi-
mation or Soil Taxonomy. This system classifies soils on the basis of
diagnostic properties and diagnostic horizons. Diagnostic properties
include soil temperature, soil water availability, soil mineralogy,
and soil chemical or physical properties which are all measured in the
field or easily obtained through laboratory tests. The presence of
certain diagnostic horizons and properties are influenced by soil de-
velopment processes. Problems occur when minesoils are classified
using the Soil Taxonomy because man's influence on soil development
is not currently recognized in the definition of diagnostic horizons.
For example, soft rock fragments common in minesoils are not often
observed in natural soils. As a result soft rock fragments must be
grouped with lithic rock fragments, but their influence on soil re-
sponse is very different. In natural soils, the presence of excess
sodium is recognized when a natric horizon is present. However,
minesoils with excess sodium do not have natric horizons because of
their genetic youth, and therefore sodium in minesoils cannot be
formally recognized. Fortunately, Soil Taxonomy was designed to
allow changes so that new soils can be formally classified. One
approach to classify minesoils would be to formulate new family
criteria which recognize the unique properties of minesoils. With
this approach, most but not all, minesoils would be Entisols. Mine-
soils in this study would be Typic Ustorthents. To formally classify
minesoils at higher levels of Soil Taxonomy, new diagnostic horizons
and properties will need to be defined which recognize man's influ-
ence as a soil-forming factor. At the present time, the best way to
classify minesoils is to define them at the series and phase level.
The soil series is the lowest level which is recognized in soil
classification, and as such limits of soil properties can be narrowly
defined. The soil phase is based on recognition of properties in
the field which affect management but are not considered in soil
classification. Soil phases are useful for mapping minesoils because
of their flexibility.
~enesis
1.
Reclamation methods such as application of "topsoil" create minesoils
similar in some respect to undisturbed soils. These techniques simulate
hundreds to thousands of years of soil development on raw spoils. No
reclamation techniques produce minesoils identical to natural soils,
however. Differences between mined and unmined landscapes need to be
recognized to properly manage reclaimed land.
2.
Controlled burning or grazing should be investigated as management tech-
niques for preventing litter accumulation which immobilizes nitrogen
and organic carbon in the developing soil system. These techniques
will accelerate the breakdown of litter, narrowing the CIN ratio, and
may ultimately enrich the organic matter content of deep soil layers
by promoting greater root growth.
9
-------
3.
The man-influenced origin of minesoils has resulted in several unique
properties not commonly observed in undisturbed soils. Minesoils in
Colstrip have a high volume of soft weatherable rock fragments that
supply water to plants but prevent root penetration. Fragments break
down in the upper 20 cm of mine soils in 50 years. These fragments act
in part like rock and in part like soil. Soil texture is continuously
modified by their breakdown over a long period of time, especially where
shale fragments occur in sandy soil. The role of soft rock fragments in
mines oils is not yet understood. Abrupt changes in texture are a common
occurrence in minesoils. These stratifications or pockets of texturally
contrasting material could strongly influence water, and solute movement;
and root growth. Research on water movement in stratified media should
be applied to minesoils.
4.
Federal strip-mine reclamation regulations (OSM, 1977) requires that the
A horizon of pre-existing soils must be salvaged for "topsoiling".
Selected overburden can be substituted for the A horizon if it can be
shown to be of equal or better quality. Overburden used as "topsoil"
did not have as favorable soil properties for plant growth as did A
horizon material in this study. Overburden was lower in organic matter,
water-holding capacity, and nutrient levels. More than 50 years would
be required for some overburden to become as suitable as salvaged A
horizons.
5.
Federal regulations (OSM, 1977) also require that the B and part of the
C horizon of soils be salvaged and re-applied if necessary to obtain
soil productivity in the root zone compatible with the final land use.
In this study, overburden should in many cases be as productive or more
productive than the C horizon of pre-existing soils. Overburden should,
therefore, be a suitable medium for use in the base of the root zone
(from 2 to 6 feet) in the Colstrip area. If applied topsoil and the
underlying spoil differ by more than two classes in texture, however;
the topsoil/spoil interface may restrict rooting. Abrupt textural
changes should be avoided in the upper 4 feet of reclaimed soils to
create an adequately deep root zone.
6.
Topsoiled mine soils appear to be more erodible than similar natural
soils before mining. This could be due to loss of soil structure, plant
cover, and the disruption of soil pores in the reclamation process. To
prevent excessive erosion; lower slopes, shorter slope lengths, and
rapid vegetation establishment should be emphasized. Reduced highwalls
present a major erosion hazard because of moderately steep, long slopes.
Preservation of intact highwalls (Murray, 1978) may mitigate erosion
problems in these situations.
Water Relations
1.
Reclamation techniques should be aimed at building minesoils with physi-
cal properties in the root zone similar to natural soils. Compacted
layers and abrupt changes in texture which may limit root penetration
for plant communities to develop which are similar to those before
mining.
10
-------
2.
Moderately rapid infiltration rates are not sufficient to prevent erosion
on minesoils. Rapid establishment of a plant cover and reduced slope
and slope length are necessary to prevent excessive erosion of mined land.
Sandy soil textures favor rapid infiltration but also result in lower
water-holding capacity. Intermediate textures such as loam, sandy clay
loam, and sandy loam may represent the best combination of favorable
water-holding capacity with adequate infiltration rates.
3.
Water is used by plant communities on new minesoils dominated by intro-
duced perennial grasses and shrubs mostly during early spring through
early summer. More efficient use of water during the summer could result
if more warm-season species are established in reclaimed plant communi-
ties.
Root Activity
1.
Common range plants in the Colstrip area have roots to nearly 2 meters
on both minesoils and undisturbed soils. Therefore reclamation tech-
niques should be aimed at providing a 2 meter root zone free of com-
pacted layers limiting to root penetration and chemically suitable for
root growth.
2.
Root activity varies from year to year and is influenced by extremes in
the soil environment such as low temperature and low soil water poten-
tial (dry). It appears that three to four years are required for the
root system of plant communities on reclaimed land to resemble root
biomass and distribution prior to mining. Supplemental irrigation
during the developmental stages of plant communities may increase the
chances for successful vegetation establishment during adverse years.
11
-------
SECTION 4
LITERATURE REVIEW
Soil Genesis
A soil consists of a vertical sequence of layers or horizons, each with
a unique combination of properties such as: pH, organic matter content, tex-
ture, and mineralogy. Jenny (1941) stated that the arrangement, kinds, and
properties of horizons in soils are the result of five soil-forming factors.
These factors are climate, organisms, parent material, relief, and time.
Jenny further proposed that each factor had an independent effect on soils.
In the past 35 years, numerous studies on single factors of 80il formation
have been conducted (Birkeland, 1974).
Other workers have proposed different approaches to the study of soil
development. The independent influence of a single soil-forming factor is
often difficult to isolate in nature. Hole and Nielsen (1970) suggest that
the "factors" combine and interact to produce general "processes" of soil
formation (Simonson, 1959). These processes acting through time on a newly-
forming soil produce distinct properties. For example, the process of
"melanization" produces a thick, dark, A horizon high in organic matter
content. Likewise, the processes of eluviation and illuviation tend to
either remove soluble salts and CaC03 from the profile or produce distinct
layers of these materials deep in the profile.
Early Stages of Soil Genesis - Classic Studies: Initial stages of soil
development have been studied on dune deposits (Salisbury, 1925; Jenny and
others, 1969; Olsen, 1958), Mt. Shasta mud flows (Dickson and Crocker, 1953a,
1953b, 1954,) and glacial till (Crocker and Major, 1955). All workers found
that vegetation strongly influences initial soil development. Ulrich (1956)
and Yaalon (1975) emphasize the importance of parent material in determining
the properties and genesis of young soils.
Dickson and Crocker (1953a, 1953b, 1954) studied soil development and
vegetation succession on Mt. Shasta mudflows from 27 to 1200 years old.
Organic carbon, total nitrogen, pH, and bulk density changed rapidly during
initial soil development and were strongly influenced DY vegetation. Total
organic carbon and nitrogen in the soil and litter increased to a maximum in
200 years. A gradual flux of total C and N progressed from litter to soil
for 500 years. Bulk density, pH, C, and N approached "steady state"
(Birkeland, 1974) levels in the soil in 200 to 500 years. A similar pattern
of soil development was found in recent glacial till in Alaska (Crocker and
Major, 1955), and in northern California sand dunes (Crocker, 1967). Total
nitrogen reached a maximum in 100-year-old glacial till then decreased,
12
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instead of approaching a "steady state" value as in the other chronosequences.
Olsen (1958) studied soil development on a sequence of Lake Michigan
sand dunes 0-12,000 years old. Organic carbon and nitrogen in the upper 10
cm rose quickly in the first 300 years, and more slowly until steady state
was approached in 1,000 years. CaC03 content was initially 1.5 to 2.0
percent in the sand but was nearly removed from the upper 10 cm of the soil
in 600 years. The average depth of leaching of CaC03 was 2 m after 6,000
years. Silt and clay content rose from near zero initially to an equilibrium
level in 1,000 years. Silt and clay content again increased in 8,000- to
l2,000-year-old soils probably as a result of loess deposition during the
Pleistocene.
Parsons and others (1962) investigated soils on Indian mounds of known
age in Iowa. He compared relative profile development of 1,000 to 2,000-
year-old mound soils to undisturbed soils on 14,000 year old loess. Horizon-
ation developed most rapidly in the first 1,000 years of soil development.
Al horizons reached maximum expression in 1,000 years, while 2,500 years were
required for pronounced soil structure to form and clay translocation to
become evident. Bilzi and Ciolkosz (1977) found cambic horizons in 200-year-
old alluvium and 40-year-old mines oils (Ciolkosz and others, 1977) in
Pennsylvania. They reported that 2,000 years were required for argillic
horizon formation in Oregon while more than 5,000 years were required in New
Mexico.
The general pattern of soil development is for levels of properties to
change quickly during initial stages then change less rapidly as equilibrium
is approached. The amount of time required to reach equilibrium is different
for each property. Organic matter, pH, and total nitrogen can change quickly
in soils (100-500 years). Carbonate movement requires more time (>1,000
years), while clay movement may require 2,000 to 10,000.
Minesoil Genesis: Smith and others (1971) studied soil genesis in
iron-mine spoils in West Virginia. Spoils had deeper rooting, higher cation
exchange capacity, and higher exchangeable nutrients than natural soils.
Natural soils had lower bulk density, higher porosity, stronger soil
structure, and higher nitrogen and organic carbon contents. Water regimes
in the top two feet were similar in spoils but natural soils had higher
infiltration rates. The authors concluded that minesoils were superior to
natural soils in some respects while inferior in others. The minesoils were
expected to support woodland and pasture as productive as on unmined soils.
Wa1i and Freeman (1973) studied species composition and soil character-
istics of North Dakota mine spoils compared to adjacent undisturbed areas.
Spoils had higher pH; electrical conductivity; exchangeable magnesium, and
sodium; total phosphorus, and sulfur; and silt, and clay content. Unmined
sites had more organic carbon; exchangeable potassium; species diversity,
abundance, and density. Some mined sites did not support "desirable" plant
species 53 years after mining.
Cas pall (1975) found that organic matter content increases rapidly with
13
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time in the top few cm of Illinois minesoils. Organic matter increases more
slowly below about 5 cm. After only 14 years, organic matter in the upper
12 cm of minesoils was about 60 percent of equilibrium levels. Depths of
carbonate leaching increased from 4 cm in l4-year-old minesoils to 15 cm in
30 years.
Down (1975) reported on soil development in colliery waste tips in
England. Accelerated erosion occurred in all spoils (32°-36° slope). How-
ever, sheet and gully erosion was less rapid on spoils more than 20 years
old. Particle-size decreased with increasing age due to weathering of shale
fragments, and surface coal content also decreased with age from 54 percent
initially to 2.5% after 178 years. An ameliorative effect of fine coal
fragments on soil structure and nitrogen status was noted.
Anderson (1977) investigated changes in glacial till mine spoil in
Saskatchewan ranging from 28 to 40 years in age. Soluble salts had been
leached below 50 cm, and lar~e amounts of carbon and nitrogen had accumula-
ted. Humus in 28-year-old minesoils was very similar to that found in
natural soils.
Soil Development in the Northern Great Plains: McKeague and St. Arnaud
(1969) state that water movement is the most important phenomenon in soils
leading to profile differentiation. Components of soil vary in their
mobility with moving water. Mogen and others (1959) found successive accumu-
lations of carbonate, gypsum, and soluble salts with increasing depth as a
result of differential mobility in North Dakota soils. Redmond and Omodt
(1967) studied till-derived chernozem soils in eastern North Dakota.
Dominant soil development processes included organic matter accumulation;
structure formation; leaching of soluble salts and carbonates; color changes;
and formation of finer-textured B horizons due to clay eluviation and in situ
clay formation. Curry (1975) suggested that the development observed in
Northern Great Plains soils are a remnant of a wetter climate several
thousand years ago. The results of Anderson (1977) and this study (Schafer
and Nielsen, 1978; Schafer, and others, 1977) indicate that many of the soil
development processes outlined above are active in 50-year-old minesoils .
Minesoils should become more like natural soils with increasing age since
the same procp~ses which have occurred in the development of natural soils
are active in minesoils.
Soil Water Relations in Spoils
The availability of water for plant growth is one of the primary limit-
ing factors in reclamation of western mined land (NAS, 1974). The amount of
water available for plants depends on precipitation, infiltration, run-off,
and water movement into or out of the base of the root zone. Several workers
have studied these and other factors influencing water movement in mine-
soils.
Infiltration: low infiltration rates on minesoils cause increased run-
off which can reduce plant available water, remove applied topsoil, and
create sedimentation problems. Erosion and reduced infiltration are there-
fore major problems in arid mine land reclamation.
14
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Gilley and others (1976b, 1977) measured run-off and erosion on native
range, and topsoi1ed, and non-topsoi1ed spoils in North Dakota using a large
rainfall simulator. Two storms of one hour duration and 2.5 inch/hour inten-
sity were simulated. Soil loss on native range was 200 kg/ha; only 12% of
the applied water ran off the plots. Water from both events moved deeply
into the profile (>18 inches).
Soil loss on raw spoils was 15,000 kg/ha and 21,000 kg/ha on cultivated
and uncultivated erosion plots. Run-off consisted of 66 to 74% of the
applied water. Water did not penetrate significantly into uncultivated
spoils and increased only in the upper 6 inches of cultivated plots. . Culti-
vation of the topsoil/spoil interface did not increase percolation into the
spoils. As slope was decreased from 17 to 6%, soil loss was reduced by about
30%. Differences in spoil texture had little influence on soil loss.
Erosion was greatest on topsoi1ed spoils at 74,000 kg/ha. As topsoil
thickness of the treatments was increased from 25 to 61 cm, run-off decreased
but erosion increased. Water content of the topsoil zone increased after the
rainfall events, but no water entered the underlying spoils. Application of
straw mulch decreased erosion on topsoiled and non-topsoiled plots by 93 and
84% respectively.
Erosion was less on spoils without topsoil because a surface crust
formed on the clayey sodic materials which slowed erosion. Topsoil materials
on spoils were more erodible than similar undisturbed soil in part due to a
loss of soil structure during the handling process (Gee and others, 1976).
Water content of topsoil increased rapidly during the rainfall events.
Gilley and others (1976a) found that eroded material from uncultivated spoils
had a particle size distribution similar to the surface spoil. Sediment from
the cultivated plots had less sand and more clay than the spoil.
Miyamoto and others (1977) reported that some spoils in New Mexico were
non-wettable and as a result had slow infiltration rates. High-grade coal
was identified as the source of the hydrophobic substance. Addition of ethyl
alcohol significantly increased infiltration into coaly spoil by decreasing
the contact angle thus increasing capillary adsorption. Infiltration into
sodic, non-coaly spoils was not affected by addition of ethyl alcohol, but
was increased by adding CaC12 to the irrigation water. Miyamoto (1978)
tested several wetting agents to evaluate the feasibility of increasing
infiltration on coaly spoils. Only anionic-type compounds significantly
increased spoil wettability. The effectiveness of anionic sulfonate may have
been due to the anion adsorption capacity of low pH coal.
Arnold and Dollhopf (1977) found that minesoils in southeastern Montana
had slower 30 minute infiltration rates than undisturbed soils. The presence
of vegetation or application of topsoil significantly increased infiltration
into spoils, however. Dollhoptand others (1977) found a similar result on
spoils at Colstrip and Savage, Montana; and Beulah, North Dakota. Infiltra-
tion on selected surface soil treatments decreased in the order topsoil/
chiseled> non-topsoil/chiseled> topsoil/dozer basin. The dozer basin
treatment removed topsoil from the basin area, and in addition compacted the
underlying spoil. Therefore, infiltration was highly influenced by the
15
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surface material and decreased from topsoil to spoil to compacted spoil.
Wyatt (1978), working with data from this study, found that infiltration
rates on native range, old spoils, and new spoils were not significantly
different. Spoils and soils were predominantly sandy loam in texture and
were non-sodic. Application of topsoil derives its maximum benefit when the
spoils are clayey, sodic, or high in coal content. Although topsoil often
increases infiltration, and can store more water than spoils; it is very
erodible with a small amount of run-off and therefore must be protected
during the early stages of reclamation.
Water Use and Movement: Once water penetrates the soil surface by
infiltration it can move downward under the influence of gravity, upward or
downward in response to matric potential gradients, or be used by roots. The
interaction of these processes and others causes water to move differently in
different soils. Water movement and plant use of water has not been exten-
sively studied in minesoils .
Dollhopf and others (1977) studied the water balance at three Northern
Great Plains strip mines under five different erosion control treatments.
They found that water recharge was greatest on topsoiled plots. Dozer basins
were the most effective surface manipulation for increasing recharge. Water
content in the upper 50 cm was at a maximum in February. Upward vapor
movement of water to the frozen soil zone was postulated to occur as a result
of temperature gradients (Ferguson and others, 1964; Willis and others,
1964). Water was used most rapidly from June to August. Soils remained dry
through most of the fall. Evapotranspiration averaged 75, 57, and 47 cm per
year at Savage, Montana; Colstrip, Montana; and Beulah, North Dakota. A net
upward movement of water from below the root zone (250 cm) occurred at most
sites. It was not known whether upward movement of water would cause salt
accumulation.
Curtis (1973) measured the water content and density of former ridge and
valley locations in a regraded Kentucky stripmine. Former spoil ridges were
more compacted and contained less water than valleys. Compaction may have
been due to the compressive weight of the spoil material or vehicle traffic
during regrading. Surface density on all spoils decreased during the first
winter after deposition probably as a result of frost action.
Arnold (1977) found that the hydraulic conductivity (K) of native range
soils (4.9 cm/day) was greater than all spoils studied (1.3 cm/day). Top-
soiled spoils had higher K values in the topsoil zone than in the underlying
soil. Drainage below the root zone of fallow native range and spoils was
calculated. Assuming the soil was recharged to field capacity in the spring,
2.5 to 4.0 cm would drain in one year from spoils and native range respec-
tively-
Gilley and others (1976a) found that topsoiled spoils had higher infil-
tration than raw spoils. However, water did not penetrate the topsoil-spoil
interface. Cultivation of the interface to increase contact did not influ-
ence percolation into the spoils. Restricted percolation of water below
the topsoil zone was also observed by Do11hopf and others (1977). It was
16
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suggested that physical and chemical treatments to decrease compaction and
minimize clay dispersion would be necessary to increase deep percolation.
Henning and Afflect (1977) in Iowa found that deep tillage of compacted spoil
sub layers increased infiltration, deep water movement, and initial corn
growth.
Grassland Root Systems
The underground portions of plants comprise one of the most important
components of an ecosystem as well as the most difficult to study (Troughton,
1957). Several methods have been used to study root weight and length; and
the seasonal dynamics of live, dead; functional, and senescent roots.
Knowledge of the maximum rooting depth of range plants is important in
planning mine reclamation. Minesoils should be created which provide a root
zone sufficiently deep to support the reclaimed plant community. The root
zone should be free of physical barriers to growth and chemically harmful
zones.
Methods: One of the most straightforward methods of characterizing
roots is to excavate a trench and sketch the root distribution observed in
the profile. A monolith can be extracted from the trench and washed free of
soil to further isolate the root system. Weaver and associates used these
methods to produce volumes of information on the distribution and depth of
roots of numerous plants in North American prairie (Weaver, 1919; 1920; 1958;
Weaver and Darland, 1949; Albertson, 1937). These methods are time consuming
and provide only qualitative information, however.
The framed monolith method is similar to the previous one in that a
large soil monolith is collected in the field and washed free of soil. After
soil removal, roots are subsampled by depth increment for obtaining root
weights. The framed monolith method is probably the most accurate but also
the most time consuming method of studying roots (Bohm and others, 1976).
Soil cores are often used instead of intact monoliths in many root studies.
Individual cores can be subsampled by depth and washed free of soil. Many
cores are necessary to measure root biomass because of the small sample size
(Schurman and Goedewaagen, 1965). Special man-operated (Brown and Thilenius,
1977) and hydraulic coring devices (Bartos and Sims, 1974) have been used to
speed sample collection. Root separation by hand is very time consuming so
that machines have also been developed to speed this process (Brown and
Thilenius, 1976). Repeated measurements of root weight have been used to
study the seasonal changes in root biomass (Bartos and Sims, 1974; Dahlman
and Kucera, 1965; Lauenroth and others, 1975; Schuster, 1964).
Tracer techniques have also been widely used for studying root systems.
These methods are well-suited for studying the changes in the seasonal
dynamics and function of roots; but are not widely used for estimating root
weight. The radioisotope p32 is most commonly used for studying roots.
Radiophosphorus can be injected at any selected soil depth, and if roots are
growing in that layer, p32 will be transported to the plant top. Thus, root
distribution can be inferred fromthe.presence or absence of p32 in harvested
plant tops (Boggie and others, 1958; Burton and others, 1954; Cooper and
17
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Ferguson, 1964; Hammes and Bartz, 1963; McClure and Harvey, 1962). Differ-
ences in root activity with depth have also been investigated by observing
differences in the amount of p32 taken up at different depths (Fox and Lipps,
1960; Lipps and others, 1957). Root distribution has been investigated by
injecting p32 directly into the plant and then measuring the radioactivity of
soil cores after the p32 is distributed evenly in the vlant (Halstead and
Rennie, 1965; Rennie and Halstead, 1965). Finally, p3Z has been used to
study translocation of materials within the plant (Racz and others, 1964;
1965; Sosebee and Wiebe, 1973).
Radiocarbon, C14, has been widely used recently to study the functional
dynamics and productivity of root systems (Caldwell and Camp, 1974; Singh
and Coleman, 1973 and 1974). The plant top is exposed to labeled C02 under
an airtight tent. After a selected period of time, roots from the treated
plant are core-sampled and measured for C14 enrichment. Other stable iso-
topes such as lithium, strontium, and rubidium have also been used to study
root growth (Fox and Lipps, 1964).
Root Biomass: Several measurements of root biomass have been reported
that are applicable to the Colstrip region. Lauenroth and others (1975)
found that root biomass in the upper 10 cm of soils near Colstrip generally
increased from May through July then decreased during the fall. Values for
root biomass averaged 500 g/m2 in the upper 10 cm of some communities
dominated by Stipa aomata.
Singh and Coleman (1973) measured root biomass on Colorado short-grass
prairie dominated by Blue grama (Bouteloua graailis) and Buffalograss
(Buahloe daatyloides). Root biomass in the upper 60 cm of the soil was 1894
g/m2 of which 66% of the roots were functional as determined by C14 assimila-
tion. Bartos and Sims (1974) studied similar plant communities under
variable grazing pressure. Root weight in the upper 80 cm reached a maximum
in early summer and again in early fall. The average biomass was 1275 g/m2
in 1969 and 1702 g/m2 in 1970. Root biomass in the upper 10 cm varied most
during this period. They reported that most roots occured in the upper 10 cm
probably in response to the shallow penetration of precipitation in that
region.
Dahlman and Kucera measured root biomass during different seasons in
Missouri tall-grass prairie. Biomass varied from a minimum of 1449 g/m2 in
April to a maximum in October of 1901 g/m2. Peak root biomass occurred in
July for the 0-25 cm layer but was delayed in lower soil layers. Approxi-
mately 25% of the root system turned over each year, however, turnover rates
were lower at lower soil depths.
Caldwell and Camp (1974) measured root biomass in two cool-desert
communities, one dominated by Cera to ides lanata and the other by A trip lex
aonfertifolia. Biomass in the 0-75 cm soil depth was 1541 and 1823 g/m2
for the two communities respectively. Below-ground biomass was 7 to 11 times
that of aboveground.
Seasonal dynamics: Many workers have studied changes in root systems
through the growing season. Root weight; the proportion of live and dead,
18
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or functional and senescent roots have all been investigated
Models of root biomass dynamics have been developed based on
of C14 in the plant during different times of the year.
in this manner.
the partitianing
Root biomass in grassland ecosystems is at a minimum in early spring
before root growth initiates (Dahlman and Kucera, 1974. Biomass increases
rapidly and reaches a peak usually in mid-summer. A gradual decline in late
summer is sometimes followed by a secondary increase in the fall (Bartos and
Sims, 1974). From 12 to 25% of the root system is renewed each year in both
Missouri prairie and Utah desert communities. This agrees with the findings
of Weaver and Zink (1946) who found that root survival over a three year
period was 81, 45, 14 and 10% for Andropogon furcatus~ BouteZoua graciZis~ B.
curtipenduZa~ and Stipa spar tea respectively.
Singh and Coleman (1974) measured both root biomass and the percent of
functional roots with depth. The proportion of functional roots decreased
from around 70% in the upper 10 cm to 30% at 60 cm. This probably resulted
from slower decomposition at depth. The specific activity (~Ci/g roots) of
roots from each depth was used to isolate zones of potential growth or
storage of assimilate. Growth below 40 cm was most rapid early in the grow-
ing season. It was postulated that growth of deep roots was important for
utilization of soil water. Specific activity of roots from 10 to 20 cm
increased through the growing season. It is likely that photosynthate was
being stored in these roots for use as energy reserves during the following
year. Roots at this depth were observed to begin growth early in the growing
season before any leaves had formed aboveground, which indicates the utiliza-
tion of stored carbohydrates.
Boggie and others (1958) and Burton and others (1954) found that roots
in the upper 10 cm of the soil transport over ten times more p32 to plant
tops than do roots at deeper soil depths. Increased root abundance, phos-
phorus availability, or soil temperature or moisture could account for this
difference. Burton (1954) found that differences in p32 uptake from deep
soil zones correlated with root biomass distribution and drought tolerance
in several southern U.S. grasses.
Fox and Lipps (1960, 1964) studied p32 uptake by a1flafa in subirrigated
fields in Nebraska. They found three distinct zones of p32 uptake in the
soil including 1) an intermittently moist zone near the surface, 0-1.2 feet;
2) a dry, chemically inferior zone from 1.2 to 7 feet; 3) and a wet zone
above the water table from 7 to 12 feet. Early in the growing season, 88%
of the p32 accumulated from all depths came from the surface layer. Only 5%
of the p32 was taken from the surface late in the growing season, however,
when water was limiting. During this period 62% of the p32 was taken up from
below seven feet even though only 3% of the root weight occurred below that
depth.
Bartos and Jameson (1974) found that root biomass in short-grass prairie
was highest in early summer and again in early fall with a minimum occurring
in mid-summer. They explained this phenomenon by formulating a model which
recognized a decomposition process causing weight loss and a new growth
process resulting in biomass increase. Maximum decomposition was postulated
19
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to occur slightly before maximum growth accounting for the minimum root bio-
mass during mid-summer, a period of active growth. When decomposition was
set at 40% of the total biomass, which is a maximum value from the literature,
the combination of the growth and decay processes did not adequately fit the
observed data. They suggested that other processes may be involved in the
mid-season biomass minimum, or that more decomposition occurs than is common-
ly recognized. Assuming these large decQmposition rates are valid, more than
80% of total plant photosynthate would be used in new root growth each year.
Ares and Singh (1974) investigated the dynamics of root biomass under
short-grass prairie dominated by Bouteloua gracilis by modeling carbon flow
between various sources and sinks. Carbon was depleted from root crowns
early in the growing season before the appearance of new leaves for early
growth of juvenile roots. The carbon in root crowns was replenished later in
the growing season. Carbon reached a maximum in juvenile, non-suberized,
and suberized roots at progressively later times in the growing season.
Carbon in dead roots peaked in the fall and continued to increase gradually
until the following spring. Carbon in dead roots was depleted by decomposi-
tion rapidly each spring when soil temperature rose high enough to stimulate
microbial activity. Carbon lost by root respiration had a similar peak in
late spring and summer. Models such as this suggest the complexity of the
interactions of root growth, decay, and environmental conditions such as soil
water and temperature.
Microbiological Activity
Microbial activity is an essential part of the soil-forming process,
because such activity is directly related to soil aggregate stability.
Initially, a reclaimed strip mine soil (termed "spoils") would have no hori-
zon development, and one would expect to find relatively low levels of
microbial activity. As spoils progress to a state supporting plant life, the
level of microbial activity can be expected to change. Hence, the monitoring
of microbial activity near the minesoil surface may be one index of soil
genesis itself.
Recently there has been much interest concerning the measurement of the
high energy, energy transfer molecule adenosine triphosphate (ATP) as a means
of measuring microbial activity. ATP is found in all living systems. Within
a bacterial cell ATP concentration will remain relatively constant throughout
the organisms growth curve (Atkinson, 1971), and under most conditions is
destroyed immediately upon the death of the cell (Holm-Hanson and Booth,
1966). The measurement of ATP is based on the observations of McElroy and
Strehler (1949) who described the light emission resulting from the mixing of
ATP with heat stable (luciferin) and heat labile (luciferase) extracts from
the luminous crustacean Cypridina hilgendorfi. Since one photon of light was
emitted for every molecule of ATP, quantitative measurements were possible.
The determination of microbial activity in soils utilizing ATP measure-
ments has been an area of active research. MacLeod, and others (1967)
measured ATP concnetrations in twenty-five terrestrial soil samples, finding
values ranging from 1.2 x 10-7 to 8.0 x 10-9 g ATP/g soil. These concentra-
tions are within the range of the findings of Doxtader (1969) who detected as
20
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little as 6.0 x 10~10 g ATP/g soil. Similarly Greaves and others (1973),
while investigating microbial populations in basin peat, found ATP concentra-
tions to range from 6.3 x 10-8 to 9.4 x 10-7 g ATP/g soil. These findings
indicated that ATP was a reliable parameter in its own right, and was there-
fore used in this study as the primary means of assessing microbial activity
in minesoils.
21
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SECTION 5
STUDY AREA
Colstrip was chosen as a study area because of its relatively uninter-
rupted history of mining since 1924. Nearly level mine spoils ranging in age
from 1 to 50 years provided an ideal setting for the study.
Location
Colstrip is located in the northern portion of the Powder River basin in
the Northern Great Plains physiographic province. It lies in southeastern
Montana along the East Fork of Armells Creek which is a tributary of the
Yellowstone River 50 km (30 miles) to the north (Fig. 1). The study area was
unglaciated during Pleistocene time, but late Tertiary uplift of the region
caused downcutting of rivers and rejuvenation of much of the landscape
(Fig. 2).
Geology
Geologic history of the region since Pre-Cambrian time includes periods
of deposition, erosion, and deformation. During Paleozoic and Mesozoic time
a sequence of carbonates, sandstones, and shales was deposited (Fig. 3). The
area was a tectonically stable epicontinental sea during these periods.
Several hundred meters of clastic rocks were deposited during Cretaceous
time as a result of repeated transgressions and regressions of the sea.
Broad regional uplift after deposition of the Bearpaw Shale is believed to
have caused permanent withdrawal of marine water from the region (Gill and
Cobbin, 1973). The late Cretaceous Hell Creek Formation which overlies the
Bearpaw Shale is of fluvial and lacustrine origin (Lewis and Roberts, 1977).
Subsidence of the present Powder River Basin began during deposition of
the Hell Creek Formation in late Cretaceous time (Curry, 1971). Subsidence
corresponded to the beginning of the Laramide orogeny during which the Black
Hills and Big Horn Mountains bordering the basin were uplifted. The lack of
coarse clastics and conglomerates in late Cretaceous and Paleocene deposits
suggests that major uplift of the Big Horn Mountains and Black Hills didn't
occur until Eocene time. At the close of the Cretaceous, large amounts of
material were being deposited in swampy flood plains of the newly-formed Pow-
der River Basin (Lewis and Roberts, 1977), setting the stage for deposition
of the Paleocene Fort Union Formation.
The Fort Union Formation is divided into the Tullock, Lebo, and Tongue
River Members in southeastern Montana. Other workers treat these as forma-
tions in the Fort Union Group (Curry, 1971; Jacobs, 1973). The basal Tullock
22
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CANADA
YELLOWSTONE R.
MONTANA
SCALE
=-
o 00
WILES
;'
;'
;'
./
/
;'
I
/
/
/
/
/
/
I
\
\
\
\
\
\
.;;,P-" ../ - -
,....--
'"'
...
.\.
rig. 1. Map showing Colstrip study area location and
LANDSTAT-1 image of the region (NASA).
23
NORTH
DAKOTA
SOUTH
DAKOTA
-------
Fig. 2.
Typical landscape in the Colstrip area.
Member of the Fort Union contains an abundance of sandstone and thin coal de-
posits. Sediments were deposited in a fluvial environment of low topographic
relief with abundant temporary ponds and marshes (Lewis and Roberts, 1977).
Intervals of erosion and nondeposition are common in this member as inferred
from abrupt truncation of cross-bedding, and channel sands cutting across
shale and coal beds. The Lebo Member consists of shale and mudstones depos-
ited in a similar environment. Locally, the Lebo Shale was derived from
lacustrine processes. Deposition of the Lebo Shale corresponds to a period
of rapid subsidence of the Powder River Basin. Uplands which currently
border the basin were not yet a significant sediment source (Curry, 1971).
The Tongue River member of the Fort Union Formation contains some of the
most extensive reserves of coal in the world. In western North Dakota,
Tongue River sandstones are mostly fine to very fine grained sub angular sub-
graywacke commonly showing a characteristic "salt and pepper" speckling
(Hickey. 1977). The dominant cement is calcite. The degree of induration
depends on the amount of cement, but most rocks are weakly cemented. Lime-
stone sand grains are common indicating exposure of carbonate rocks in the
sediment source area (Jacob, 1973). Claystones in the Tongue River Member
contained a mixture of illite and kaolinite with lesser amounts of smectite.
In western North Dakota, four primary lithologic associations are common
in the Fort Union Formation (Jacob, 1973). 1) Gray clay and silt units from
1 to 30 feet thick with disturbed stratification, and thin coal stringers are
common. These represent floodplain deposits in a low relief fluvial environ-
ment. 2) Thick coal seams often overlie the gray silt and clay units and
represent a swampy floodplain zone of deposition. The tabular blanket-like
geometry of these seams may indicate a lower delta plain origin for the Fort
Union in western North Dakota. 3) Yellow silt and sand deposits up to 50
24
-------
ERA
U
tI
~
0- ~
u
,
500-
1000-
u
~
"I
1500- ~
IV
VI
~
~
~
~
II.
~ 2000-
U
2500 - ~
Iii
-J
~
1-
3000 - <:
~
~
~
~
1
I
PERIOD
TERTIARY
CRETACEOUS
JURASSIC
TRIASSIC
PENNSYLVANIAN
MISSISSIPPIAN
DEVONIAN
URIAN
OROIVICIAN
CAMBRIAN
AQUIFER
COMPLETE STRATIGRAPHIC
COLSTRIp' MONTANA
SECTION
(DNR8C
1974)
(AFTER
VAN VOAST
ET AL. 1977)
EPOCH
o
MEMBER
FORMATION
TONGUE RIVER
\
\
\
\
I
\
TONGUE RIVER \
CONT,
I
S
~PI
~ ~ CHUG WATER
~ TENSLEEP
\" AMSDEN
--.. CHARLES
MISSION CANYON
LODGEPOLE
DEVONIAN L.f\JDrFF
INTERLAKE
STONEY MOUNTAIN
~T~N~~~R
DEADwOOD
e SEMENT ROCKS
.
300-
LEGEND
c=J ~ mm I!IIi CJ c:::::J
CRY$TALUNE CARBONATE SILTSTONE NlUDSTONE SANDSTONE
ROCKS ROCKS SANDY SHALE SHALE
COAL
Fig.
3.
Stratigraphic section in the Colstrip area
(Dollhopf and others,
\
\
\
Ii)
~
i-:20-
~
~
~
j;l£"LL
31-M
0-
BED
ROSEBUD
OVERBURDEN
ROSEBUD
COAL
PROBABLE
DePOSITIONAL
ENVIRONMENT
FLOOD BASIN-
NATURAL LEVU
CREYASS SPLAY
CHANNEL
(POINT 8ARS)
NATURAL LEVEE
CREV,"S! SPLAY
FLOOD BASIN
- --
ROSEBUD NATURAL LEVEE
MC KAY CREVASS SPLAY
INTERBURDEN
MC KAY
COA
--
FLOOD bASIN
---
SOURCES
MONTANA STATE DEPARTMENT OF
NATURAL RESOURCES a CONSERVATION /974
VAN VOAST, HEDGES a MC DERMOTT /977
10-
30-
----
40-
- - -
1978b) .
-------
feet thick overlie many coal seams. Sedimentary structures in this unit sug-
gest these sands originated as a natural levee and crevasse splay deposit.
These sandy units contain about 25 percent more iron than surrounding units.
Natural levees form the highest land surfaces in the floodplain. A highly
oxidized condition would be expected in this environment, favoring precipita-
tion of iron and perhaps other metals. 4) Sand occurs as linear bodies per-
haps deposited as transverse bars in low-sinuosity meandering streams. Rare-
ly, tabular sand bodies 8-10 feet thick extending for over 1000 feet later-
ally were encountered, and were interpreted as point bar deposits.
Jacobs (1973), Royse (1970) and Cherven (1978) suggest a lower flood-
plain delta environment for the Paleocene in western North Dakota. Workers
in central (Shurr, 1972), and southeastern Montana (Widmayer, 1977) postulate
a purely fluvial depositional environment without deltaic influence. Because
of the fine grain-size and paleo-current indicators in southeastern Montana,
a sediment source several hundred km to the west was suggested.
The local geology of Colstrip was described by Dobbin (1930) and Renick
(1929). Dollhopf and others (1978a, 1978b) found a complex sequence of sandy
and silty deposits overlieing the Rosebud coal seam at Colstrip (Fig. 3).
Geometry of these units suggest an origin as point bar, natural levee, and
crevasse splay deposits. Sediments are laterally inextensive over tens to
hundreds of meters which makes sampling and characterization of overburden
extremely complex.
Early Eocene time was a period of strong folding and faulting (Glaze and
Keller, 1965) which resulted in many of the present structural features of
southeastern Montana. During the Oligocene and Miocene, the area is thought
to have been buried by tuffaceous debris from volcanic activity to the west.
Regional uplift during the Pliocene accentuated many structural features
bordering the Powder River basin. Rejuvenation of streams caused previously
buried sediments to be exhumed. Erosion continued until Pleistocene time to
form the present landscape. The study area was not covered by Pleistocene
continental glaciation, however, changes in climate resulted in downcutting
of rivers, formation of river terraces, and rejuvenation of much of the land-
scape.
Soils
Colstrip lies in a soil transition zone of Aridisols, Alfisols, and Mol-
lisols. Aridisols or desert soils increase in abundance in the southern
Powder River basin where the climate is drier. Mollisols, prairie soils, are
common in the moister Great Plains of North and South Dakota to the east.
Alfisols, or forest soils, occur in the neighboring Big Horn mountains and
Black Hills regions. Entisols which are young, undeveloped soils are locally
common due to steep slopes and recent fluvial activity.
Simonson and others (1978) recognized a mixture of Camborthids and shal-
low Torriorthents in the Colstrip area on nearly level to moderately steep
dissected bedrock hills and plains (Fig. 4). Soil series typical of these
associations included Busby, Cabbart, Riedel, Yamac, Yawdim, and Twilight.
North of Colstrip, more clayey soi18 were recognized where sediment of the
26
-------
. FORSYTH
,
\
\
\
\
\
\
\
\
,
IP
LEGEND
TH2 - Entiso1s-Aridiso1s: strongly sloping to steep soils on dissected
sedimentary bedrock plains and hills.
Torriorthents (shallow) - Camborthids - Torriorthents
TH3 - Entiso1s-Aridiso1s: strongly sloping to steep soils on dissected
sedimentary bedrock plains and hills.
Torriorthents (shallow) - Torriorthents - Camborthids
TP4 - Andiso1s-Entiso1s: nearly level to moderately steep soils on
sedimentary bedrock plains.
Camborthids - Torriorthents
VH1 - predominantly clayey. strongly sloping to steep soils on
dissected shale plains.
Torriorthents (shallow) - Camborthids - Natrargids
Fig. 4.
Co1strip region soils map showing dominant soil associations
(Simonson and others, 1978).
27
-------
Lebo Shale Member are exposed at the land surface. Aridic Haploborolls and
Aridic Argiborolls with weak argillic horizons are also locally common com-
ponents of the soil landscape.
Properties observed in soils result from the interaction of five soil-
forming factors. Climate, organisms, parent material and relief, combine to
create a set of processes which modify soils through time. The soils thus
formed in turn affect vegetation, hydrology, and land-use patterns. Informa-
tion on the distribution of different kinds of soils and their individual
properties is basic to an understanding of the natural resources of an area.
In the Colstrip area, potential evapotranspiration far exceeds annual
precipitation. Run-off during snowmelt and high-intensity summer thunder-
storms prevents some precipitation from ever entering the soil profile. As a
result, Colstrip area soils are dry in the root zone during much of the grow-
ing season. Limited penetration of water into the soil causes an accumula-
tion of lime and other more soluble salts near the base of the root zone.
Many coarse-textured soils are dry long enough to have an aridic moisture
regime typical of desert soils. Finer-textured soils retain water longer into
the summer and have an ustic moisture regime. Some soils at low elevations
have a mesic temperature regime while upland soils have frigid temperature
regimes (mean annual soil temperature less than soC, 47°F). Climate plays an
important role in the classification of soils in the Colstrip area.
Vegetation also influences soil development. The Colstrip region is
dominated by mixed-grass prairie with Ponderosa pine savannahs in upland
areas. Soils under grassland tend to accumulate thick layers of organic mat-
ter due to the turnover of fibrous grass root systems (Mollisols). Soils un-
der coniferous forest often have an 0 horizon of relatively undecomposed
litter underlain by a leached, acid mineral A horizon. Argillic B horizons
(clay accumulation) are also common in forest soils (Alfisols).
Composition and texture of parent material affect soil properties espe-
cially in "young" soils. The Tongue River Member of the Fort Union Formation
outcrops through much of the Colstrip area. Sandstone dominates this member
with abundant lenses of siltstone. A sheet of clayey shale overlies the
major coal seam. Scoria (porcelainite) resulting from combustion of exposed
coal caps many buttes in the area. Coarse-loamy and fine-loamy textural
classes of soils are dominant locally. Some fine-silty soils occur on collu-
vium derived from siltstone. Skeletal and fragmental soils are common on top
of scoria capped buttes.
Both slope and aspect or exposure, influence soil properties. Due to
the sufficiently steep gradient of streams in the region, the weakly consoli-
dated nature of Fort Union rocks, and the youthful landscape; a moderately
steep dissected topography has resulted. Keefer (1974) classified the land-
surface form in the area "open high hills." Twenty to 50 percent of the land
surface has slopes less than 8%, and local relief ranges from 500 to 1,000
feet.
At this latitude (46°N). differences in aspect strongly affect microcli-
mate which influences soil development through vegetation differences. Soils
28
-------
on north-facing slopes are colder and wetter because less incident energy is
available to warm and dry these soils. More organic matter accumulates and
deeper solums develop on north- and east-facing slopes.
The rate of geologic erosion is high on steep slopes. As a result, only
thin A horizons form because soil material is continuously removed from the
surface. Steep surfaces are not stable long enough for cambic B horizons
(horizon of alteration) to form. The resulting soils are Entisols (Fig. 5).
o
Z
-
CJ)Q2>-W
510 CDZ
-U...J>-
W"".. IoJH.
'in "Vi
en :g :~f w ~
"' Z
>-:::106:0::
CD::) , ;' '0::':'" : :':'i\::, " ,"., , ,". ,',', ' ' , ' ..' . ~.~ ,
ROCK .";::':',';:,'::\::.>,:,:<,::,', '," ,,~I "
. " " >--.,....;:....;:...., CI '
~~
'0
W
0::
~
:I:
en
t-
Z
ILl
>
=>
...J
I£.
SLOPE
..,.~... C2
. ' , ""J,, ALLUVIUM
t "i~";'_-> ':;'~;~_:t::.
PROFILE
R
Representative slope profile and soil series which develop
on various parent materials at each geomorphic position
in the Colstrip, Montana area.
On midslopes, surfaces are more stable. Cambic B horizons form and thicker
A horizons accumulate creating Borollic Camborthids. On the lowest foot-
slopes where slope flattens, material carried by overland flow from upslope
is deposited due to a loss in energy of moving water. Retention of surface
run-off in this geomorphic position results in more water moving through the
profile than in other soils. Thick mollic epipedons and some argillic hor-
izons may develop. Aridic Haploborolls and Aridic Argiborolls are common.
In recent floodplains, materials are periodically reworked which prevents B
29
-------
horizons from forming.
These stream-influenced soils are Fluvents.
Climate, organisms, parent material, and relief together create processes
which modify soils through time. The length of time a surface is exposed to
soil-forming processes thus influences the degree to which many soil proper-
ties are expressed. Pleistocene glaciers did not reach the Colstrip area,
however, changing Quaternary climates has probably influenced these soils.
Uplift of the entire region in Pliocene time began a cycle of downcutting by
rivers which has rejuvenated the soil surface in recent times. Most soils in
the area are probably near 10,000 years old.
Vegetation
Most native vegetation in southeastern Montana consists of either mixed
prairie or coniferous woodland plant associations. Ross and Hunter (1976)
list dominant species in the potential climax plant communities in the Col-
strip area. These include western and thickspike wheatgrass, little bluestem,
needle and thread, green needlegrass, bluebunch wheatgrass, big bluestem, and
prairie junegrass. Shrubs should include silver sagebrush, skunkbush sumac,
winterfat, and western snowberry. Under grazing pressure blue grama, prairie
junegrass, fringed sagewort and others are expected to increase in dominance.
Mixed prairie is dominant in the Colstrip area, and is composed of a
diverse mixture of warm and cool season perennial grasses, forbs, and shrubs
(Dollhopf and others, 1978). Overgrazing has commonly occurred in the Col-
strip area which has promoted development of increaser and invader shrubs,
half-shrubs and weedy forbs. Grasslands in the Colstrip area are generally
sub-climax in nature.
Mixed prairie sites produce from 1000-1800 kgfhafyear, with mean produc-
tion near 1250 kg/ha/year (Munshower and DePuit, 1976). Livestock carrying
capacity varies from 1.5 to 13 A/Aum. A limited amount of native rangeland
has been converted to agricultural land uses including hay pasturage and
cereal grain production. The primary land use in the area, however, consists
of livestock grazing.
Climate
A continental climate influences the Colstrip area. The extreme range
in recorded temperatures from -40°F to 111°F characterizes this climate.
Despite high summer temperatures, large diurnal temperature fluctuations
moderates mean daily temperature to 71.5°F during July, the warmest month.
Average annual precipitation for the period 1941-1970 was 40.1 cm (15.8 inch-
es) (NOAA, n.d.). Thirty centimeters of precipitation falls during the April
to September growing season with 15 cm coming early in the growing season.
Summer precipitation occurs as showers and high intensity thunderstorms.
Annual precipitation can deviate substantially from the average 15.8 inches.
Only 8.6 inches fell in 1934 while 24.7 inches was recorded in 1944 (Table 1).
Geologic evidence accumulated in the northern Rocky Mountains, and mid-conti-
nent regions suggest that the climate has changed dramatically in the last
10,000 years during the time when most Colstrip soils were forming (Morrison,
1965). Following retreat of the Wisconsin glaciers and again 4,000 years ago
30
-------
the climate was colder and wetter than than today, while during the "alti-
thermal" period of 6,000 years ago, a warm dry climate existed. The climate
today is somewhat cooler and wetter than during the Altithermal period.
Table 1. Annual precipitation at Colstrip, Montana for the years
1928-1977 (NOAA, nd).
YEAR PPT (in.) YEAR PPT (in.) YEAR PPT (in.)
1941 17.7 1962 15.3
1942 18.3 1963 17.8
1943 17.7 1964 18.5
1944 24.7 1965 14.3
1945 13.8 1966 13.0
1946 20.9 1967 17.2
1947 11. 3 1968 19.8
1948 16.4 1969 17.6
1928 12.1 1949 11. 9 1970 15.6
1929 12.0 1950 14.6 1971 19.2
1930 12.0 1951 14.8 1972 16.6
1931 11.3 1952 10.1 1973 16.9
1932 20.4 1953 19.3 1974 18.4
1933 18.2 1954 11. 3 1975
1934 8.6 1955 17.5 1976 12.7
1935 15.7 1956 13.6 1977 16.1
1936 10.9 1957 18.4
1937 12.0 1958 17.0
1938 12.3 1959 10.5 average 15.4
1939 14.3 1960 10.4
1940 19.7 1961 14.7
Land Use
The dominant land use in the Colstrip area is livestock grazing on the
extensive grasslands of the region. An increasing amount of land around the
townsite is being used for urban development including single and multi-
family dwellings, schools, commercial developments, parks, and roads. Power
generating plants and associated settling ponds, cooling ponds, pipelines,
and service roads occupy several hundred acres. Many small tracts in broad
valleys are used for cereal grain production. Finally, a limited amount of
land along subirrigated perennial stream courses is used for dryland produc-
tion of alfalfa and other hay crops.
31
-------
Site Selection
Research sites for intensive study were chosen to represent spoils depos-
ited throughout the history of mining at Colstrip. In addition, undisturbed
sites were selected for study of baseline soil characteristics and processes.
Changes in mining methods through time, depth and type of overburden moved,
and reclamation methods applied resulted in a variety of spoils with widely
varying characteristics to choose for study. Differences in soil development
processes and land use patterns similarly caused a diversity of undisturbed
sites. Two criteria were used to select research sites: 1) sites should
extend over the widest variation in properties observed and 2) some sites
should be selected to represent the modal or most common characteristics.
Research sites were selected during preliminary field investigations by
personnel familiar with undisturbed soils of the area, mining history, and
reclamation methods. Fifteen sites were chosen for intensive study. These
included 1) five undisturbed native range sites on common soils of the region,
2) five sites on old spoils which were formed between 1928 and 1948, and 3)
five sites on new spoils in a recently active mine area where modern reclama-
tion techniques were applied (Fig. 6).
A detailed description of each site on spoils was prepared including
type of overburden material, mining methods, age, seeding mixtures, fertili-
zation, other reclamation techniques, present vegetation and management.
Characteristics of undisturbed sites included type of material, soil classi-
fication, landscape position, and dominant vegetation (Table 2).
A companion study to evaluate vegetational succession on mine spoil
shared many of the research sites (Sindelar and Plantenberg, 1977). Detailed
description of vegetation composition, and production were made available for
comparison with soil properties.
32
-------
R41E R42E
:0
)
~
T2N
TIN
I
I ,/
. T:-
COLSTRIP AREA
LOCATION OF STUDY SITES
----- -
= SECONDARY HIGHWAYo
,
- IMPROVED ROAD
- - - - - UNIMPROVED ROAD
--------- RAILROAD
. STUDY SITE
o STRIP-MINE AREA
5
MILES
o
~~
KM
o
N
SCALE
I 72000
WMS ./1.
Fig. 6.
I~cation of 15 research sites near Colstrip, Montana.
The site names represent either the soil series if na-
tural soils, or date of last disturbance if minesoils.
33
-------
Table 2.
Description of origin, characteristics and management of re-
search sites. Sites were chosen to represent the diversity
of characteristics as well as typical aspects of minesoils
and undisturbed soils in the Colstrip area.
2.!!!.
Chlnook-!
9.!h!!
Boxwell-2
Ethridse-4
R1edel-6
Chinook-8
1948-)
1928-5
1928-7
1928-9
1929-10
1915-11
1973-12
1'17 :-1)
1969-14
197u-15
~
Thta dte is located 1n .. toulope
landse.ape position on " norch-facing
slope. The 5011 11 an Arid1c:
Hap!oboroll and hAs . buried soU at
1 III. It 18 . very youthful 1011.
The site \188 cultivated at some
time in the past.
This site l1u in a 1I1dllope podtion
on an upland surface. The 8011 11 .
Haploboroll and has a well expressed
Coo
The 8011 1, .. Borollic Kaplu&ld.
It lie. 1n ill toea lope padUan and
ha. developed 1n c:olluvlua from
shale. GYPSU8 and soluble salt!! are
prelent below 1 II. The site "'a.
cl,lltivated some t1.ae in the recent
put.
The 11011 18 a IIhaHeN BaroUte
Camborthid and ha. .. par.lithic
contact at 50 cm. It 18 on .. heavy
level interf lure and haa developed
in vell.l(ly consolidated 8and.tone.
This site 18 in a 81ddle backslope
pOsition. The aoU is an Ar idic
Haploboroll and haa developed frOft
.and.tone colluviUli. The solum i.
aixed due to rodent burrowin,
activity.
p,\,. soil contains coal-rich material
or "~ob" from the pit bottom. Coal
t rapents and shale are cOlDOn.
The site was created in 19::fI and
C(ln.l.t5 of excess surface overburden
material reJ'IQved frail. the 8ine area.
It i8 nearly level and was derived
from 9andstone and colluviUII. Soft
rock fraRfl\ents are cOl'llllon below
10 em.
Sa=e as 1928-S
Same .. l'JZ~-'">
The site was created in the S8lllt:
wav a, 1')28-5 but the material 18
mort: clayey. Shale fragment. are
connon.
Thi. nearlv level site wa. topsoiled
wi th 10 em of sandy materh 1. The
upper 80 em of the solum loIa9
deposited with scrapers. Scoria
fraRftlents are cOf!l'lon at the surface.
Shalr.'-rich lavers are conanon
throughout the profile.
No topsoil vas applied to this site.
!'Iaterial was deposited with bull-
dozers. Sandstone frali(r!ent<, are
Ten to 15 cn of topsoil was applied
on this nearly level site. The
upper 100 cm of the profile wu
deposited with scrapers. Shale-rich
lavers are common in the profile.
()ld unTegraded spoils from previous
minlng were regraded by bulldozer
in 19&9. No topsoil w,n applied.
Shale and coal fragment are common.
ThlS nearly level site was deposited
by bulldozer. No topsoil was
applied. Sandstone rock frapents
are cOCllbon.
VeRetation
A mixture of grasses and
forbs is dominated by Stipa
~on:zta, :...:-e:en-l ~"stata,
and ':;":-...c~.<.Y..-.1 ?1',J~"':13.
81'"O"fUB sp. 1s COllCOn
locally around pocket
gopher holes.
Stipa C'c.r-;;::zt..~ Al"'istida
tongise ta. and Tragopogon
dubius dominate the St.and.
Annual grasses are
abundant.
Al'teMe8ia ~aJ1Q. Gutierr,ulia
8al'Othrae. and Ariatida
~onQiaeta are dominant
components of the
vegetation.
BoutetoU/2 :;N~l: "'[I~ Ko.t.l"'i4
G'nstata. >ttF'Q ~ornata and
several forbs dominate th1a
overgrazed site.
8outelOka gNG'l:.a, Ko.t.l"'ia
~ristata. 3tipa C'~'rout'l. and
CatQ11lovi lfa ~(,>1~::r, ;'6: LJ are
do.inant 8ra.ses. ..;....; r~~81 ~
psilost.achya and other forbs
are COl8BQn.
Poa pNtnlsis. Stipa "L'''''lt..l~
and several other forbs.
and shrubs are dominant.
Al'tef'lesia draG'lQ1C'uluolll and
annual grasse. dominate
the stand.
A. .iraC'W1,-~ :14. and A. oona
along vith .:t1F'u CoP'ICIta
and Ag1'Op!iJ"O'l 81'JitJaii are
doninant.
Several perenni8l arasses
and forbs are connon on
this site.
A}r"-"'r yl'OJ'l spicat..,., 18
dominant vith other perennial
grasses. forbs, and shrub..
Veaetation vas sparae
in 1976 and 1977.
Temporary stabilizers
and Sal.ola. kali vere
domin.8nt.
~,!r~-'rjrVI"J ~1"'is::.at..r.
,;. ~<":'>';'7..1tW"'~ Br..:-r-rv.e
tl'lemi8: and 'Ie~',-~Qgc<
S.Jt:.va comprise most of
the veKetation.
Similar to 197)-12
~!Jl'0pYl'OJ1 ':"1Ac/8taG'hyUf'l. A.
~~;~~~:d visG'idiflO1"uB
Similar to 1973-12
~
none
none
none
none
Mixture of 10 grasses.
1 shrub, and 2 leaUfDea
vas drill seeded.
~ixture of 23 grasses
drill seeded.
3 gra.aea. leluse. and
vheat vere broadcast
se.eded. A broad seed aix
vith 24 .pecies vas
drilled.
Ten Ira.ses. 2 shrubs,
and 3 le,un.s vere drill
seeded.
lVelve gra.se., 2 shrubs,
and 3 legumes vere drill
seeded.
Reclamation Treatment
FertiUzation
185 kl/ha of 06-20-0)
ft.rtilizer appUed on
4/76
188 kg/ha of (16-20-0)
applied in hll, 1975
or apring, 1976
5/72 (84-56-0) ka/ha
~;7~' (:~i;l~~~; '20;
4/74 (90-121-22).
4/70 112 kg/ha of
(16-20-0)
11/70 (84-179-67);
1/72 (168-121-0);
4/74 (90-121-0);
7/74 (45-56-22)
none
none
louginB surface
ma.nipulation
louged
34
-------
SECTION 6
MATERIALS AND METHODS
Fifteen sites were chosen for intensive study on old spoils, new spoils,
and undisturbed native range. Fences were constructed at each location to
protect research areas from disturbance by livestock and to comply with fed-
eral regulations governing use of radioactive isotopes. Research activities
were located within the fenced exclosures as shown in Fig. 7.
\"GATE '"'U ~-- ----
~ (J c c
PIT FOR SOIL SAMPLING
c
PSYCHROMETERS
(15,50,75, 150 em)
18.3m
60 ft. 0 NEUTRON ACCESS TUBES
c 6 I:::. I:::.~o-
(25m)
p32
.s- METAL POST
01
RESEARCH AREA ~~. 3 STRAND BARBED-WIRE
WOODEN POST
o C
----------------
FENCE
C
o
PLOT
DESCRIPTION
Fig. 7.
Arrangement of research exclosures.
Soil Characterization
Excavations two meters deep were made with a backhoe at each site to
allow detailed description of soil pedons and collection of bulk soil samples
from the profile face (SCS, 1971). The National Soil Survey Laboratory in
Lincoln, Nebraska and the Montana SCS state office assisted in description
and sampling of each pedon in August, 1976. Pedons were described in the
field by experienced soil scientists using standard terminology used in soil
survey (Soil Survey Staff, 1962). Bulk samples were collected from each
35
-------
horizon for laboratory analysis. In addition, samples were collected separ-
ately from narrow depth increments near the soil surface. Detailed surface
sampling was intended to isolate small changes in soil properties which may
have occurred only in the upper few cm of spoils during 50 years of soil de-
velopment. Native soils were identically sampled to insure proper comparison
between minesoils and undisturbed soils. Undisturbed clods were obtained
from selected horizons for measurement of bulk density, and water retention;
and for preparation of soil thin sections (Brewer, 1976).
The National Soil Survey Laboratory in Lincoln, Nebraska provided stan-
dard soil analysis of all pedons. Analysis performed on all samples included
mechanical analysis; CaC03 equivalent; pH 1:1 in H20; pH 1:2 in CaC12; organ-
ic carbon; total nitrogen; and pH, water content, and electrical conductivity
of saturated paste. For selected samples the following data were obtained:
water retention at 0.3, and 15 bars; bulk density of ovendry, and 0.3 bar
sample; clay-sized CaC03; extractable ions; saturated paste resistivity; and
total soluble salts. Clay mineral abundance was estimated for two to four
samples from each pedon. Semi-quantitative estimates of clay mineral species
was based on comparison of peaks obtained from x-ray diffraction of the ori-
ented clay fraction. Atterberg limits were measured on a few samples. Stan-
dard methods used by the Soil Survey Laboratory were followed in obtaining
the analyses listed above (SCS, 1972).
Additional analyses were performed at Montana State University on select-
ed pedons which were most representative of native soils; and old, and new
spoils. Total phosphorous was determined using the method of Muir (1952) as
suggested by Syers and others (1968). Inorganic phosphorous was fractionated
according to the procedure of Chang and Jackson (1957) into Al-P, Fe-P, Ca-P,
reductant soluble P, and occluded Al-P. Phosphorous concentration in each
extract was determined colorimetrically according to John (1970). The dif-
ference between the sum of inorganic P fractions and total P was assumed to
represent organic P. Analysis of DTPA extractable Cu, Fe, Zn, Mn, (Follett
and Lindsay, 1971), Ni, Cd, and Pb was also performed. Modifications of the
DTPA procedure were observed (Soltanpour and others, 1976).
A quantitative estimate of the "parent material" of each minesoil was
obtained by measuring the content of different rock types at 50 cm in each
minesoil pedon. A point count technique was used to measure the volume
of differing materials (Daniels and others; 1968). Three sets of 100 counts
each were averaged to obtain an estimate of the "parent material" for each
pedon.
Rock fragment content decreased towards the surface of minesoils. This
decrease suggested that rapid weathering of some rock fragments was occurring.
To estimate the susceptibility to weathering of different kinds of rock frag-
ments, pebble counts and visual volume estimates of fragments were made at
several depths in spoils.
Water Movement
Seasonal patterns of water movement were evaluated by measuring soil
water content and soil water potential at monthly to bi-weekly intervals from
36
-------
June, 1976 to September, 1977. Daily precipitation records for the period
were obtained from a NOAA weather station at Colstrip. Other components of
the water balance; run-off, deep percolation, and evapotranspiration were
not directly measured.
Water content was measured by the neutron moderation method (Long and
French, 1967). A Troxler model 1255 neutron probe with an americium-berylium
neutron source was used with a model 2601 Troxler scaler for all measurements.
Three access tubes two inches in diameter were installed at each of 15 sites
to a depth of 210 cm. Volumetric soil water content was measured 22 times
during the study. Water content was measured at 15 cm intervals from 0-90
cm, and at 30 cm intervals below 90 cm. Factory calibration was used to cal-
culate water content from field measurements. Changes in the total amount
of water stored in soils, and patterns of water removal and recharge were in-
vestigated.
Double-junction thermocouple psychrometers (Chow and deVries, 1973) were
installed to measure soil water potential and soil temperature. Psychrome-
ters were located at 15, 50, 90, and 150 cm and were read at the same time as
the neutron probe. The sensors were oriented horizontally to avoid tempera-
ture gradients which would bias measurements (Wiebe and others, 1977). A
Kiethly model 155 microvoltmeter and Emco switchbox were used to read the
psychrometers. During the winter of 1976-1977 all psychrometers were return-
ed to the lab for cleaning and calibration over NaCl solutions of 2.3, 13.4,
31.5, and 45.5 bars. Psychrometers were read three times over each solution
at 20°C. The calibration results were fit to a curve of the form.
E = A (1-e.000726 ~)
where E equals the psychrometer reading in microvolts, ~ is the theoretical
potential of the solution, and A is statistically derived by a least squares
curve-fit. The form for this equation was derived from Rawlins (1972) who
calculated the EMF response of an "ideal" psychrometer:
EMF = 882.6 (l-eVw ~/RT)
Values of A which were empirically derived averaged 692 with a standard devi-
ation of 107, and were in most cases less than the theoretical value of 882.6.
A theoretical correction for variations in ambient temperature was used to
adjust water potential measurements obtained in the field. A factory cali-
bration was used to calculate soil temperature from psychrometer readings.
Infiltration velocity was determined at three positions on each site in
August, 1976. A rainfall simulator which applies water droplets over a 0.31
m2 area from 50 cm above the soil surface was used (Meeuwig, 1971). A flow-
meter. registered .the rate of water application which simulates an intense
storm in volume, but not raindrop impact. Run-off was measured at four-minute
intervals. The difference between application rate and run-off was equal to
the infiltration rate.
37
-------
Root Biomass and Activity
Three different methods were used to characterize root systems at the
research sites. The number of exposed roots exposed in a standard area of
soil were counted; roots from three depths were sampled, separated from soil,
and weighed; and radioactive phosphorous, p32, was injected at selected
depths. Uptake of p32 by roots was indicated by radioactivity of plant tops
measured at several dates after injection. This combination of methods al-
lowed measurement of root biomass and also seasonal dynamics of root activity.
Standard field description of soils include an estimate of root abundance
as absent, few, cornmon, or many. These terms correspond to a range in the
number of roots exposed in a dm2 area (Table 3).
Table 3.
Abundance of roots by number and size (from Soil Survey
Staff, 1975).
Very Fine Fine Medium Coarse
Class « 1 unn) (1-2 mm) (2-5 rnm) (5-10 mm)
average number per square decimeter
Few < 10 < 10 < 1 < 1
Common 10-100 10-100 1-10 1-5
Many >100 >100 >10 >5
A more accurate estimate of root abundance was required for this study
than few, cornmon, or many. Therefore, the actual number of roots in each
size class were counted at five randomly selected locations at each of three
soil depths; 10 cm, 50 cm, and 100 cm. The above classification of root
sizes was expanded to include microfine roots from the smallest visible dia-
meter to 0.5 mm in size. Results of this counting method were correlated
with actual root weights so root count data which are quickly obtained in the
field can be correlated to root biomass which is more physically meaningful.
Schafer and Nielsen (1978) report additional details and results of the root
count method.
Decimeter cubes of soil and roots were collected at each location where
roots were counted as in the previous section. These soil cubes were return-
ed to the lab where roots were washed free of soil by washing on a 1 mm sieve.
Roots collected from each cube were weighed after 48 hours drying at 60°C and
again after ignition at 600°C overnight. Root weights are reported on an ash-
free basis.
A radioactive tracer, p32, was also used to investigate the be1owground
portions of plants (Boggie, and others, 1~~8; Burton and others, 1954, and
Lipps and others, 1957). Injections of P were made at approximately one
foot intervals to seven feet. If plant tops exhibited an increase in beta
radiation after injection, it was assumed that growing roots were present at
the injection depth.
38
-------
On June 10-11, 1976, six p32 injections were made at 13 research sites.
The tracer was placed at 15, 46, 76, 107, 137, and 183 cm. Injection holes
were prepared by driving a tempered steel rod to the desired depth. Holes
were spaced 3 m apart to avoid interference between injection sites. Injec-
tion sites were selected near several different dominant plant species so that
p32 would be available for uptake by existing root systems.
The p32 solution was prepared by diluting carrier-free p32 in HCI solu-
tion with 2.2 x 10-3 ! KH2P04 and 2.4 x 10-2 ! HCI to a final concentration
of 0.10 mCi ml-l. A leur-Iok syringe was connected to a suitable length of
steel tubing to deliver 2.0 ml of tracer solution at the desired depth. After
injection of p32, the tubing was rinsed with 5 ml of distilled water and 5 ml
of air before removing it from the hole. This method results in a 5-10 cm
diameter radioactive sphere of soil (Ferguson, 1976).
Radioactivity of plant tops within 1 m of the injection hole was measur-
ed in situ on June 27, July 14 and August 10. Beta radiation was measured
with an anti-coincidence Geiger-Muller (G-M) detector and scaler (Duncan and
Ohlrogge, 1957) designed and constructed for this study (Fig. 8). The Gei-
ger-Mueller detector and counter were designed by Dr. J. Amend, Chemistry
Dept., MSU. The engineering research lab unit built the field unit.
35mm
92 ~ mm dlQm cap
( Threaded)
ANTI- COINCIDENCE GEIGER-MUELLER
DETECTOR
(ALL METAL PARTS ARE STAINLESS STEEL)
SCALE
~
o 20mm
~mm
...~ Adjustable Dose leo'
64 mm dlom
Fig. 8.
Anti-coincidence detector.
39
-------
A schematic diagram of the detector and circuitry appears in Fig. 9. Use of
an anti-coincidence system allowed accurate field readings by reducing error
from background radiation. A Thyac G-M survey meter was used to locate ra-
dioactive plants near the injection hole. Three one-minute counts were taken
with the anti-coincidence detector on each date. If plants were only slight-
ly radioactive, one ten minute count was taken. After the last field measure-
ments in 1976, plants were harvested to obtain readings by Liquid Scintilla-
tion Counting (LSC) in the lab. Plants were dried at 110°C for 24 hours,
ground, dry-a shed , dissolved in a LSC emulsifier and counted in a Tri-carb
LSC spectrometer. In this way field readings with the anti-coincidence de-
tector were correlated with standard LSC readings (Wyatt, 1978).
ANTI - COINCIDENCE
CIRCUIT
-y .01,1 KV
-=-
~
HV
+5
-= Schmitt
Trigger
Interfece
1 Mini.cond
(Disable Pulse)
To
Counter
-
+5
~
Diodes IN749A
300 psec
Delay
Pulse
10 psec
Count
Pulse
HV
Fig. 9.
Schematic diagram of circuitry in anti-coincidence detector.
In 1977, 10 research sites were injected with p32. Three injections
were made at all depths in each of three sites which were representative of
native range, old spoils, and new spoils. This replication allowed the sta-
tistical reliability of the radioactivity measurements to be estimated. Most
injections were made on March 24, 1977; however licensing requirements limit-
ed the amount of undiluted p32 which could be kept on hand. A second injec-
tion was therefore made on A~ril 6, 1977 to obtain the desired number of
sample sites. 0.2 m Ci of P 2 was placed at the same depths as 1977, but in
addition an injection was made at 214 cm. Plant radioactivity was measured
as in 1976 on the following dates; April 16, April 30, May 14, May 31, June
17, July 9, July 19, and July 31. Several plants outside the injection area
were also measured to obtain background levels of beta radfation.
40
-------
Radioactive phosphorous has a half-life of 14.3 days. When plant radio-
activity is measured in situ on successive dates, some of the radiation re-
corded on a given date could be caused by residual p32 retained in the plant
since the previous measurement date. Since the decay rate of p32 is known,
however, this residual radioactivity could be calculated and subtracted from
field measurements. The corrected field count would give an indication of
p32 taken up only since the previous injection. Further correction of the
field counts could be made for p32 decay since the original injection. This
final value would allow comparison of uptake for each time increment between
injections. If we assume that changes in radioactivity in plant tops are
caused by differences in root growth rate or "root activity," then comparison
of corrected radiation measurements would provide a measure of the seasonal
dynamics of root growth of individual plant species at different depths. A
general view of the belowground functioning of each site could also be ob-
tained. An equation was derived to make these corrections (App. C).
Microbiological Activity
Sample collection: Soil samples were collected on August 9-12, 1976, on
June 10, 1977 and on October 10, 1977. The methods of taking each set of
samples follows.
August 1976 samples were portions of the samples taken by a collabora-
tive team effort from freshly dug pits. The sampling depths and manner of
sampling were dictated by the necessity for soil classification and analysis
and are described elsewhere. For microbial activity, portions of the sieved
and mixed samples were placed in plastic bags and immediately frozen on dry
ice. This was done within 5 to 10 minutes of sample preparation and there
should have been very little loss in microbial activity. A total of 118
samples were collected.
Samples were collected in June, 1977 with a 5.1 cm (2 inch) soil corer
to a depth of 30.5 cm (12 inches). in triplicate at each site. Each of 45
cores was divided into three 10.2 cm (4 inch) sections (designated as top,
middle and bottom sections), placed in plastic bags and frozen on dry ice
within three minutes of coring.
Samples from 54 cores were taken in an identical manner in October, 1977.
An additional 14 soil samples were collected with a preponderance of plant
roots in order to determine ATP activity in free soil, rhizosphere and rhi-
zoplane samples. These 14 samples were dug with a spade to an approximate
depth of six inches but with no regular dimensions. One gallon samples were
taken to obtain a clump of roots of a single plant with as much adhering soil
as possible. These samples were frozen on dry ice as soon as collected.
All samples were kept in a freezer chest with dry ice during transporta-
tion to the laboratory and then stored in a freezer.
Microbial activity: ATP was used as
Each soil sample was treated as follows:
shell dry blender. A sample was removed
this being one gram for the 1976 samples
the indicator of microbial activity.
Soils were blended in a P-K twin
to determine dry weight equivalent,
and five grams for the later samples
41
-------
where more soil was available. Triplicate samples, 100 grams when possible,
were weighed out and the ATP extracted. This was accomplished by mixing with
boiling O.lM NaHCO) in a one gallon Waring blender using 18 parts by weight
of bicarbonate solution to one part by weight of soil. From each mixture of
soil and bicarbonate, triplicate samples of 19 ml each were removed by pipette
and centrifuged at 12,500 rpm and at 0-5 C for ten minutes to remove particu-
late matter. The supernate was decanted into 27 ml of iced pH 7.8 Tris buf-
fer, mixed by inversion of the tubes five times and an aliquot then placed in
a cuvette and frozen in a dry ice-acetone bath. This gave nine measurements
of the ATP for each depth at each site. ATP was measured with the Dupont
luminescence biometer standardized against known ATP preparations and results
were expressed as femtograms ATP per gram dry soil. (1 fg = 1 x 10-15 grams).
For separation into free soil, rhizosphere and rhizoplane the following
procedure was adopted: Approximately 100 g cores were spread on a paper and
the roots picked out by hand, leaving the free soil. The roots were washed
in a weighed volume of water. The material removed by washing was designated
rhizosphere and the washed roots designated rhizoplane. Dry weights were cal-
culated for all three fractions and ATP was expressed both as fg ATP/g mater-
ial (free soil, rhizosphere or rhizoplane) and as percent of the total ATP in
the 100 gram sample.
42
-------
SECTION 7
SOIL DEVELOPMENT AND CHARACTERIZATION
Chemical and physical analysis of soils in native range, old spoils, and
new spoils illustrates the soil genesis process in spoils, and also quanti-
fies broad differences between minesoils and native soils. Minesoils are
different from surrounding soils not only because of their youth but also be-
cause of their unique origin through the mining process.
Colstrip History
Mining methods, reclamation techniques, types of equipment, and even
climate have changed during the period of time when coal has been mined at
Colstrip. These changes along with soil genetic changes have resulted in
striking differences between old and new spoil~.
Coal was first mined commercially at Colstrip in 1924 by the Northwest-
ern Improvement Co. to supply coal for engines of the Northern Pacific Rail-
road. Foley Brothers Construction performed the mining under contract to
Northwestern Improvement (Fig. 10). Mining ceased in the mid-1950's but
Fig. 10.
Foley Bros. mining operation at Colstrip in 1928.
resumed in 1968 when the Western Energy Company purchased the mine and the
town of Colstrip. During 1971 to 1973 Burlington Northern Railroad leveled
and reseeded many spoils formed during the early mining period. Several un-
disturbed remnants of spoils from 1928 and 1929 were used for this study.
43
-------
Many of these spoils were removed by mining in 1978.
Coal shovels used in the early mining period could remove a maximum of
14.3 m (47 feet) of overburden material. In areas where this thickness was
slightly exceeded, excess overburden was removed with smaller shovels; side-
dumping haul trucks then deposited the material outside the mine area
(Fig. 11). The first overburden removed was deposited near the crest of a
ridge. Later material was deposited beyond the initial overburden until a
wedge-shaped platform of spoils was constructed that was flat on top (Fig. 11).
Fig. 11.
(Left) spoil platform being deposited with a side-dumping Mack
truck in 1929, (Right) material for 1929-10 site was stripped
from the right side of photo and dumped on the left.
The flattened configuration provided an ideal setting for a soil genesis study
because it prevented the accelerated erosion common on the "normal" unre-
graded spoils of that period (Fig. 36). Unregraded spoils deposited during
early mining had more clayey textures and steeper slopes than flattened
spoils of excess overburden investigated in this study.
Excess overburden from the top one to eight meters of the geologic col-
umn represented the parent material of flattened spoils constructed during
1927 to 1931. This material was derived in part from existing soils while the
remainder was from the oxidized portion of the overburden above any aquifers.
Some old spoils examined in this study had up to 10 percent by volume dark-
colored material derived from A horizons of pre-existing soils. The origin of
old spoil material is in direct contrast to newer spoils. In recent mining,
large draglines were used which have a tendency to invert the geologic col-
umn. Materials were derived largely from below the oxidized zone of the over-
burden. A thin veneer of salvaged "topsoil" was often placed on top of newer
spoils. These differences in origin might be expected to result in differing
chemical characteristics of old and new spoils. Much care needs to be taken
in this study before differences between spoils can be attributed to genetic
processes.
44
-------
In accordance with current reclamation law, many steps are involved in
the reclamation of strip-mined lands. Spoils are routinely regraded, top-
soiled, deep-chiseled, fertilized, and seeded to attain a vegetative cover.
By contrast, no reclamation was practiced on old spoils. Revegetation occur-
red only by invasion and natural succession. The proximity of seed sources
and the intensity of grazing were, therefore, critical to the revegetation of
old spoils (Sindelar and Plantenberg, 1978).
Old spoils were deposited in 1927 to 1929. Precipitation was below nor-
mal from 1929 to 1931 which could have slowed or prevented development of a
significant plant cover. The "great drought" occurred a short time later
from 1934 to 1938 (Table 1). Precipitation was far below normal, and warm
dry winds caused large dust storms. Colstrip was extremely susceptible to the
drought and dust storms because of sandy soil textures and overgrazing by
sheep and horses beginning in 1880. Many natural soils in the area are non-
calcareous throughout the solum except for a thin calcareous layer at the
surface which may be dust deposited during the mid-1930's. An aerial photo
of Colstrip taken in 1931 reveals that the old spoils were nearly devoid of
vegetation (Fig. 12). The influence of vegetation represents one of the most
b .'~'~
~"P.~
. .
Fig. 12.
1931 Aerial photo taken of 1928 spoils showing vegetation.
important soil-forming factors, expecially during early stages of soil genesis.
We can assume that the soil development process was extremely slow during the
45
-------
10 years immediately following deposition of the old spoils because of a scar-
city of vegetation.
Soil Morphology
Natural soils and minesoils are distinctly different in gross morphol-
ogy. Natural soils have formed from homogeneous parent material within the
scale of a pedon which is evident in the C horizon as weathered sandstone and
siltstone, or colluvium derived from these materials. Soil development pro-
cesses have modified these parent materials so that distinct horizons have
developed. Thin A horizons 10 to 20 cm thick have formed with dark colors
and granular structure. From about 15 to 50 cm, natural soils usually have
a cambic B horizon which has higher color value and chroma than the A horizon.
Prismatic or subangular blocky structure has formed in this horizon. Some
natural soils have accumulated enough clay in the B horizon for it to be
termed argillic. Calcium carbonate has been leached from natural soils to
form a Cca horizon with segregated lime below 50 cm. Boxwell-2 and Ethridge-
4 (Appendix A) are natural soils which exhibit profile differentiation caused
by soil development. Other processes such as rodent burrowing tend to homo-
genize soils and destroy distinct horizons (Riedel-6 and Chinook-B).
Minesoils are formed in heterogenous parent material (Table 4). A mix-
ture of sandstone and siltstone fragments of varying hardness is deposited in
a matrix of loamy sand to clay loam material formed by the breakdown of rock
fragments because of blasting during mining. Similar mixtures of fragments
are oriented in diagonal bands in old spoils because of the method used in
building these platforms. Horizontal bands of lithologically similar mater-
ials 20 cm thick are common in new spoils where scrapers were used in regrad-
ing the spoils (1971-11, 1977-13; Appendix A). New spoils regraded with
bulldozers or draglines have a uniform mixture of fragments throughout their
depth (1970-15 Appendix A). Weathering and soil formation has modified the
mixture of parent materials in 50-year-old spoils. Thin A horizons have
formed, and weakly consolidated rock fragments have disintegrated into soil.
The mixing and breaking down of fragments indicates that cambic B horizons
are beginning to form in minesoils.
Table 4.
Composition of minesoils (%) based on 3 point counts
counts each) at 50 cm depth. Several different types
fragments occur inminesoils .
(of 100
of rock
Unconsolidated Soft
SITE Matrix (%) Sandstone
1928-5 45.6 39.9
1927-7 65.9 21.5
1928-9 57.4 34.3
1929-10 63.2 3.1
1948-3 59.4
1969-14 51.0
1970-15 83.8 6.8
1972-13 66.9
1973-12 65.0 13.2
1975-11 61.4
Silty
Shale
Rock Fragments (%)
Hard
Sandstone
Porce1anite
Coal
Al Horizon
Fragments
2.1
0.3
6.1
11.7
12.2
1.3
27.1
32.1
28.2
4.9
4.5
12.5
38.6
6.6
25.1
4.2
3.4
2.0
8.5
18.9
0.3
2.0
7.3
46
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Carbon and Nitrogen Profiles
Figure 13 shows the range in organic carbon content with depth in native
soils; old, and new spoils. Native soils contain more organic carbon than
spoils between 10 and 100 cm. Old spoils, however generally contain more
organic carbon above 10 cm and below 100 cm. Litter builds up quickly in the
highly-productive pioneer community on old spoils causing a rapid increase in
soil organic matter in the upper 1 to 2 cm. Mixing of pre-existing A hori-
zons into old spoils during deposition may have caused the increased organic
carbon levels below 100 cm. New spoils also show an increase in organic car-
bon in the upper 5 cm. This may be due in part to application of "topsoil"
ORGANIC
CARBON (%)
0.1
20
4.0
6.0
o
SYMBOL SOIL TYPE
k:::::::d "NATlVE"SOILS
[[Ill]] OLD SPOILS
~ NEW SPOILS
-
E
(,)
.......
50
J:
.....
a..
W 100
o
150
Fig. 13.
Range in organic carbon content of natural soils and mine
soils.
derived from surface horizons of pre-mine soils. Old spoils contain more or-
ganic carbon at all depths than do new spoils. This increase results from
decomposition of grass and shrub roots over the 50 year period since deposi-
tion of old spoils. Organic carbon accumulates rapidly in the top 1 cm of
spoils to equilibrium levels after 50 years (Table 5). Accumulation is much
slower below 10 cm; 200 to 400 years may be required for organic carbon to
reach a steady state level (Fig. 14). Dahlman and Kucera (1965) found a sim-
ilar pattern in Missouri tall-grass prairie; 110 years were required to reach
47
-------
organic matter equilibrium in the upper 25 cm compared to 590 years for the
50-75 cm zone.
Table 5.
Organic carbon accumulated at various depths in soils at Co1-
strip. Natural soils have less carbon in litter and a small-
er C/N ratio than minesoi1s .
Organic carbon accumulation Fraction of
0-1 cm 2-5 cm 10-20 cm 0-100 cm OC in litter CIN
Natural soil .321 .435 .92 5.43 1 10
Old mine soil .363 .243 .11 1.47 23 17
New mine soils .208 .033 .00 .58 29 16
Anderson (1977) found rat~f of carbon addition to glacial-till minesoi1s
in Saskatchewan (28.2 g m-2 yr ) similar to those in this study (25.6 g m-2
yr-1 Schafer and Nielsen, 1977). However, nitrogen accumulation was nearly
twice as fast (2.43 g m-2 yr-1, in Saskatchewan; 1.48 g m-2 yr-1 in this
study). The disparity in carbon and nitrogen addition rates resulted in wide
carbon/nitrogen ratios in minesoi1s in Colstrip compared to local natural
soils. Wide C/N ratios may have resulted from the high production of pioneer
plant communities coupled with a delay in litter decomposition. As a result,
large amounts of litter accumulated on old spoils which tied up a large frac-
tion of the total carbon and nitrogen in the ecosystem. Microbiological
studies indicate nearly equal populations of heterotrophic organisms near the
surface of minesoi1s and natural soils (Hersman, 1977). A large fraction
of nitrogen in revegetated spoils may have been utilized by microorganisms in
digesting the large carbon source in litter, making nitrogen less available
for the plant community. Reeder and Berg (1977) found a similar lack of min-
eralized N after incubation of Cretaceous shales with wide C/N ratios. Lack
of available (mineralized) nitrogen in spoils may be the cause of succession-
al stagnation of some plant communities at a half-shrub/annual grass sera1
stage (1928-5). The old spoil resembling native range most in vegetative
character (1929-10) has nearly twice as much total C and N in the system, with
a smaller fraction of these elements immobilized in plant litter. Processes
which prevent litter accumulation such as fire or grazing may be necessary to
prevent immobilization of nitrogen and successional stagnation of plant com-
munities. Intensive N fertilization of newer spoils delays but does not pre-
vent litter accumulation and decreased production (DePuit and Coenenberg,
1978). Fertilization does reduce wide C/N ratios and promotes plant growth.
Subsequent litter build-up causes stagnation of the plant community unless
the site is harvested, grazed, or burned periodically.
Phosphorus Fractions
Samples from three pedons representative of old spoils, new spoils and
natural soils were selected for fractionation of phosphorus. Total P was
measured as well as several different forms of inorganic P. Organic P was
48
-------
AGE (YEARS)
10 100 1000 10000
I
I
I
- I
It) MINE SOILS I NATURAL SOILS
~ 5 I
I
C'I I
~ I
- I
5 4 I
I
I
CD I
a: I
« I
u 3 I
I
I
U I
- I
Z I
« 2 I
I
'" LITTER I
a:
0 SOIL
o
Fig. 14.
Organic carbon accumulation through time showing fraction
in litter.
calculated as the difference between total P and the sum of inorganic P frac-
tions (Table 6).
Aluminum-and iron-phosphates as well as occluded aluminum phosphate, and
reductant-soluble phosphate each comprised a small fraction of the soil
phosphorus. Few differences existed between soils in the magnitude of each
fraction. The relative amount of iron- and aluminum-phosphate, and occluded
aluminum phosphate was greater in the upper 1 cm of each soil. A reduction
in pH at the surface along with carbonate removal may have caused a transfor-
mation of soil P into these fractions. Calcium phosphate is the dominant
inorganic form of P in all soils. Organic P also comprises a large component
of total P in these soils. However, organic P does not decrease with depth
as does organic matter content. The organic P fraction which was calculated
by difference may, therefore, also include a component of insoluble inorganic
P not affected by the extraction process.
The dominant form of phosphorus in nearly all unweathered parent materi-
als is a calcium phosphate, apatite (CaS(F, C1, OH) (P04)3). During the soil
development process, calcium phosphate is often converted to iron- and alumi-
num-phosphates; and organic phosphorus. Therefore, a comparison of the
amounts of soil phosphorus in each fraction provides an index of soil maturity
49
-------
(Walker and Syers, 1976).
Table 6.
Site
Old
Mine
Soil
(1928-9 )
Natural
Soil
(Chinook-8)
New
Mine
Soil
(1973-12)
Fractions of inorganic and organic phosphorus in a typical old
minesoil , natural soil, and new minesoil (Chang and Jackson,
1957).
Depth
(cm)
1-2
5
10
15
50
100
200
0-1
2
5
10
25
50
100
150
200
0-1
2
5
10
50
80
100
200
Al
-P
34
31
16
19
16
16
16
P-Fractionation*
80
53
46
25
28
28
25
22
22
80
46
16
25
14
16
16
14
Fe
-P
Ca
-P
Red
-P
20
20
35
20
20
13
13
Oc-
Al-P
p-ppm
19
22
29
12
19
19
22
20
20
20
28
20
6
20
28
28
29
22
26
12
19
48
26
26
33
ORG-P
110
273
302
244
190
80
30
171
288
208
o
247
257
150
218
209
194
198
266
177
240
220
182
125
Tot
-P
397
544
560
504
465
346
301
464
531
464
190
459
500
405
268
473
558
477
522
432
473
455
446
338
Free
Fe%
.18
.17
.13
.14
.18
.03
.10
.20
.19
.17
.23
.23
.09
.27
.22
.12
.16
.15
.01
.18
.14
.21
.03
.15
*Phosphorus fractions include aluminum phosphate, iron phosphate, calcium
phosphate, reductant soluble phosphate, occluded aluminum phosphate, or-
ganic phosphorus, and total phosphorus.
15
15
15
15
15
7
15
199
183
163
194
205
211
205
20
20
20
20
20
35
20
20
36
29
22
12
19
19
19
5
Williams and Walker (1969a, 1969b) studied phosphorus transformations in
a chronosequence of New Zealand soils. They found that calcium phosphate
decreased rapidly to near zero in the soil development sequence. Apatite
weathered from the profiles more rapidly than feldspar, hornblende, or vol-
canic glass. Although some P was removed from the profiles, most calcium
phosphate was converted to secondary iron- and aluminum-phosphate; and with
extreme maturity to occluded phosphate. Organic P reached a peak during in-
termediate stages of soil development. All soils in this study are genetic-
ally young soils when compared to the New Zealand chronosequence. Because of
the semi-arid climate, the pH of Colstrip soils is high enough so calcium
18
18
18
18
18
15
11
15
18
146
130
146
130
127
146
173
159
1.63
34
11
15
15
7
11
15
15
194
173
183
183
173
154
194
159
50
-------
phosphate remains the primary inorganic form. The calcium-phosphate fraction
of these soils may contain apatite~ octa-calcium phosphate~ and phosphorus~
precipitated on calcium carbonate surfaces (Russell~ 1973).
Syers and others (1969) studied two New Zealand alluvial soils radiocar-
bon dated at 650 and 6500 years B.P. The youngest soil had an organic phos-
phorus distribution similar to that found in this study. Organic P did not
decrease with depth as did organic matter content. Organic P as well as sec-
ondary inorganic phosphorus were more concentrated in the fine particle-size
separates of the New Zealand soils. Primary apatite-phosphorus was most
abundant in the fine sand fraction.
John and Gardner (1971) found a decrease in calcium phosphate with in-
creasing soil age in Canadian alluvial soils. A parallel increase in iron-
and aluminum-P and organic-P was also noted. The amount of calcium phosphate
was highly correlated with the Bray-2 soil test for phosphorus (Bray and
Kurtz~ 1945).
Calcium phosphates are relatively unavailable at the pH found in these
soils. The dominant phosphorus-containing species are probably octa-calcium
phosphate and apatite which provide very little P to solution (Russell~ 1973).
As a result, most minesoils in the region are considered deficient in phos-
phorus (Power and others, 1978). Bowman and Cele (1978) stress the importance
of organic P as a plant-available phosphorus source in western soils.
Mobile Soil Components
Soluble salts: Electrical conductivity (EC) of all soils in the Colstrip
area is low (usually <1 mmho/cm). Values as high as 4 mmhos/cm were found
near the surface of new spoils and below 100 cm in native soils, however.
Between 10 and 40 cm~ natural soils have lower EC than old spoils~ which in
turn have lower EC than new spoils (Fig. 15).
The EC of some natural soils increases below 100 cm indicating that salts
accumulate near the base of the root zone. Old spoils below 10 cm have uni-
form EC values between 0.2 and 0.4 mmhos/cm. The material was initially low
in salts. Dollhopf and others (1978) found that the upper 5 to 10 m of over-
burden often is the most saline with EC greater than 4 mmhos/cm. Since old
spoils were derived mostly from below ridges in the landscape, it is possible
that overburden beneath these positions are free of salts in the upper 10 m.
A similar pattern of salt distribution was found at several North Dakota mines
by Moran and others (1978). Some new spoils approach 0.2 mmhos/cm between 10
and 100 cm but increase to 1.0 mmhos/cm below 100 cm. This salt distribution
may result from the rapid leaching of salts to the base of the root zone.
Anderson (1977) found that salts in minesoils were removed from the upper 50
to 100 cm after 30 years. This finding contradicts the suggestion of Curry
(1975) that disruption of the Northern Great Plains ecosystem by mining would
cause salts to move upward and accumulate at the surface of minesoils.
Soluble salts in natural soils consisted of nearly equal amounts of Ca++
and Mg++ with small amounts of Na+ and ~ (Appendix A). The dominant anions
were HC03- and S04-2. Below 100 cm in natural soils~ EC was higher than in
51
-------
EC {mmhos/cm}
0.1
2.0
4.0
o
50
-
E
o
-
:r:
t-
o...
W 100
o
150
SYMBOL SOIL TYPE
H::::::d "NATIVE"SOILS
ITIJIIIII] OLD SPOILS
~ NEW SPOILS
Fig, 15 ,
Range in electrical conductivity in natural soils and mine
soils.
the upper part of the profile.
tive abundance at this depth.
In addition, Mg++ and Na+ increased in rela-
In old minesoils , Ca++ was two to four
The dominant anion was HC03-, but 804-2, and
spoils than in natural soils.
times more abundant than Mg++.
Cl- were more abundant in old
In new minesoils, Mg++ and Na+ were more abundant than Ca++,
Excess
52
-------
Mg++ could compete with uptake of sufficient Ga++ for plant growth despite
the calcareous nature of new spoils (Power and others, 1978). Sulfate is the
dominant anion in new spoils, unlike natural soils and old minesoils where
HG03- is dominant. The different composition of salts in new spoils may be
caused by 1) its source within an aquifer with dominantly Mg-S04 type water
(Dollhopf and others, 1978b), or 2) weathering of pyrite and other minerals
not found in old spoils or natural soils.
All soils studied showed a marked increase in EG in the upper 1 to 2 cm
of the profile. This accumulation of salts could result from 1) evaporation
of water from the soil surface leaving a residue of salts, or 2) "base pump-
ing" or nutrient cycling of ions through the plant community. An evaporative
salt residue should be composed of a large fraction of mobile ions such as
Na+, Gl-, and N03-' Salts derived from nutrient cycling should be rich in
ions selectively accumulated by plants (such as ~). A comparison of the ion-
ic composition of soluble salts from different depths (Table 7) reveals that
~ is higher in relative abundance near the soil surface than it is deeper in
the profile. Nutrient cycling is, therefore, occurring in all but the most
recent minesoils which concurs with the suggestion of Anderson (1977).
GaG03: Fort Union sandstones are highly calcareous. Widmayer (1977)
found that sandstones in the Decker area contained 13% GaG03 mostly as dis-
crete carbonate sand grains. In this study, soils or soil parent materials
contained 8 to 14% GaG03 both as sand-sized clasts and finer matrix and ce-
ment.
The carbonate distribution in natural soils indicates that GaG03 has
been removed from the upper 30 to 50 cm of the profile and has accumulated
below that depth (Fig. 16). Spoils show a uniform GaG03 distribution through-
out the profile except in the upper 5 cm. Some old spoils have been somewhat
leached in the upper 1 cm which represents the first stages of the formation
of a carbonate distribution similar to natural soils. New spoils exhibit a
decrease in GaG03 content only where non-calcareous "topsoil" has been ap-
plied. The practice of adding "topsoil" mimics several hundred years of soil
genesis in terms of carbonate removal.
Galcium carbonate is a moderately mobile component in soils. In semi-
arid and arid regions GaG03 accumulates at various depths in the soil. Ark-
ley (1963) developed a method for calculating the time required to form hor-
izons of GaG03 enrichment based on climatic data, carbonate solubility, and
soil properties. Using this method, the time required for carbonate removal
to occur in natural soils at Golstrip was calculated (Table 8).
Variations in the age of soils can best be explained by relative land-
scape positions. The Boxwell-2 soil occurs under an upland relict surface
of perhaps early Wisconsin age. All other soils lie below a late Wisconsin
surface. Steepest slopes along interfluves on the younger surface are being
eroded most rapidly and therefore exhibit minimum ages. The Chinook-l soil
is underlain by a buried soil at 1 m and suggests recent slope activity.
The calculated age of this soil may be too high because the original CaC03
content may have been overestimated.
53
-------
Table 7. Partial ionic composition of a saturation extract is shown
from two depths for each soil. Plant nutrients such as r-
are concentrated in surface horizons which indicates nutrient
cycling has caused the surface salt accumulation observed in
these soils.
EXTRACTABLE CATIONS % OF ION
meq/1 COMPOSITION
SITE DEPTH (cm) Ca* Mg Na K TOT Ca* Kg Na K
CHINOOK-l 0-10 TR TR .5 .5 0 0 100
100-200 24.7 .1 .4 25.2 98 0 2
BOXWELL-2 0-1 11.5 7.3 .1 2.3 21.2 54 34 1 11
100-145 .6 2.1 1.0 .1 3.8 16 55 26 3
ETHRIDGE-4 0-1 12.9 11.9 .2 2.9 27.9 46 43 1 10
100-152 1.1 10.2 16.0 .2 27.5 4 37 58 1
CHINOOK-8 0-1 2.2 TR .5 2.7 81 0 19
150-200 6.3 .1 .2 6.6 95 2 3
1928-5 0-1 4.1 TR 1.2 5.3 77 0 23
100-200 4.8 0 .3 5.1 94 0 6
1928-7 0-1 2.8 TR .7 3.5 80 0 20
100-200 8.2 TR .3 8.5 96 0 4
1929-10 0-1 4.2 TR 1.3 5.5 76 0 23
100-200 9.5 .1 .2 9.8 97 1 2
1948-3 0-1 8.2 TR 1.2 9.4 87 0 13
100-153 19.4 .1 .2 19.7 98 1 1
1975-11 0-1 4.8 1.9 .2 .4 7.3 66 26 ,3 5
100-200 8.5 8.6 .5 .4 18.0 47 48 3 2
1973-12 0-1 4.7 TR .7 5.4 87 0 13
100-200 3.7 TR .1 3.8 97 0 3
1972-13 0-1 5.8 TR 1.1 6.9 84 0 16
100-200 2.9 TR TR 2.9 100 0 0
1969-14 0-1 5.4 TR .6 6.0 90 0 10
100-200 4.3 TR .1 4.4 98 0 2
1970-15 0-1 2.7 TR 1.3 4.0 68 0 32
100-200 5.4 TR TR 5.4 100 0 0
*Ca+2 was not measured in calcareous soils because of ana1ytics1 difficulties. '''hen r.a +2 values
were missing, ion composition was calculated using only the remaining cations.
Based on Arkley's method (1963), carbonate should have been removed from
the upper 2 cm of old spoils during a 50 year period. Although at least one
old spoil (1929-10) is free of carbonate in the upper 1 cm, most old spoils
are calcareous throughout the profile. Lab data and thin section evidence
suggests that carbonate is being gradually removed from the upper 10 or 20
cm rather than being completely leached initially from the upper one or two
cm. It is possible that the large grain size of original carbonates prevents
the CaC03 from entering solution rapidly enough to be quickly removed near
the surface. Instead, downward-moving precipitation dissolves minute amounts
of carbonate from successively deeper depths until water finally becomes
54
-------
CaC03
(°k)
o
4
8
12
16
20
24
o
"""""'" .
...,'0",..,.,.. .
............,... "
.............,., " .
"""""""'" . ..
"""""""'" . ..
"0""""'<"" . .. .
...........,..... . ., ..
"""""""'" . ., ..
""'0"""""" ....
""""""""" ....
,.....,.......... . ., .. ..
"'0',..,-,...... . '0 .. ..
""""""""" . ...
""""""""" . ...
'.'..0""""" . ...
""'0""'" . ....
........... . ....
"""'" . ....
""'" . ...,
-
~ 50
-
I
.....
a.
w
(:)
100
150
SYMBOL SOIL TYPE
H~~~~~~J "NATIVE"SOILS
[]]]I] OLD SPOILS
~ NEW SPOILS
Fig. 16.
Range in calcium carbonate content in. natural soils and mine
soils.
saturated with GaG03 at 20 to 50 cm. As water is later withdrawn from the
soil by plant roots and evaporation, carbonates reprecipitate at the point
where the water was removed (Fig. 17). This process continuing over several
thousand years results in the carbonate distribution observed in natural
soils.
Salomons and Mook (1976) used isotope geochemistry to study carbonate
movement in Dutch polders. They verified the process of dissolution and par-
tial reprecipitation outlined above. In the Dutch soils, about 20 percent of
the carbonate dissolved in surface horizons was reprecipitated deep in the
profile either as a result of evaporation or decrease in the partial pressure
of G02' In the more arid environment of southeastern Montana, a much larger
fraction of GaG03 (approaching 100 percent) would be expected to reprecipi-
tate. Reprecipitated carbonates should have a very fine particle size because
55
-------
Table 8.
Years required for carbonate removal to occur in five soils
near Colstrip. (These dates may vary considerably depend-
ing on how CaC03 solubility is calculated but should repre-
sent minimum estimates. Climatic data from central South
Dakota was used in the calculation, based on the method of
Arkley, 1963).
Minimum
Soil age (years) Landscape position Relative age
Chinook-1 4000 interfluve footslope recent
Riedel-6 5200 interfluve backslope recent
Ethridge-4 9300 middle backslope late Wisconsin
Chinook-8 11400 footslope late Wisconsin
Boxwell-2 32500 slope summit late Wisconsin
.,
;C;~~- N,;~OLS~
Fig. 17.
Thin section of soil pore at 100 cm in old minesoil
carbonate enrichment.
showing
of their rapid formation (Fig. 18). Old minesoils have a significant amount
of clay-sized carbonate similar to Cca horizons of natural soils (determined
by X-ray diffraction). New minesoils have very little clay-sized carbonate.
56
-------
Fig. 18.
Thin section of sandstone fragment (lower portion of
in old mines oil Fragment has large CaC03 crystals
interior but small recrystallized CaC03 around rim.
photo)
in
Dissolution of sand-sized carbonate grains may also playa major role in the
breakdown of sandstone rock fragments in old minesoils.
~: The pH of calcareous soils is usually controlled by the solubility
of calcium carbonate, carbonate equilibria, and the C02 pressure. With
normal C02 partial pressure (pC02 = 10-3.5 Atm) and pure calcium carbonate,
pH approaches 8.4 in aqueous systems (Garrels and Christ, 1965). The
presence of other soluble salts or ions such as Na+, or CaS04 can raise or
lower the equilibrium pH. Organic acids in A horizons also tend to lower pH.
The pH of most samples from Colstrip was near 8.3 reflecting the high
CaC03 content and lack of Na+ or other soluble salts (Fig. 19). Leaching of
carbonates and formation of organic acids in natural soils has resulted in a
lower pH (6.5-8.0) in the upper 50 cm. Old, minesoils show a smaller reduc-
tion in pH in the top 30 cm as a result of soil development processes. New
spoils are generally uniform in pH throughout their depths except where
"tops.oil" from the A horizon of pre-mine soils were added.
Trace Elements
Extractable levels of seven trace elements; Fe, Mn, Zn, Cu, Ni, Pb, and
Cd were measured in three soils using a DTPA extraction (Soltanpour and
57
-------
6.0
pH (I: I H20)
8.0
9.0
7.0
o
... ... ...............
.............................
...............................
................................
.................................
..................................
..................................
..................................
..................................
..................................
..................................
.................................
.................................
.................................
.................................
................................
...............................
..............................
..............................
............................
...........................
..........................
.::::::::::::::::::::::::
...:::::::::::::::::::
.....,..........
............
- 50
E
o
-
J:
t-
o.
WIOO
C
150
.
SYMBOL SOIL TYPE
b~~~~~~~d "NATIVE"SOILS
illIIIJ]] OLD SPOILS
~ NEW SPOILS
Fig. 19.
Range in pH for natural soils and minesoils.
others, 1976; Follett and Lindsay, 1971). Extractable trace element levels
have been used to determine potential phytotoxicity in stripmine spoils
(MDSL, 1977). Gough and others (1978) found that DTPA, EDTA, and ammonium
oxalate soil extractions did not predict more than 50% of the variability in
elemental concentration of range plants growing on selected soils in the
Northern Great Plains. These methods were of limited utility in predicting
plant availability. They were useful, however, in defining general ranges
in concentration which were suitable for plant growth media.
Zinc: Follett and Lindsay (1970) found that available Zn increased with
an increase in organic matter or cation exchange capacity in Colorado soils.
Less than 0.5 ppm extractable Zn was considered low for crop production. The
distribution of Zn in old, and new spoils; and natural soils is shown in Fig.
20. Extractable Zn increases near the surface of all soils perhaps due to
nutrient cycling and complexing with organic matter in surface horizons.
Natural soils and old minesoils were near the lower limit of adequate
plant available Zn below 10 cm. Zinc deficiency may be a problem in these
58
-------
o
o
DTPA - ZINC
( ppm)
4
6
2
:I: 100'0
.... .
a.. 1.1
LLJ ,:
Q :
150 'f
I :
I j
I j
200
-50
E
u
-
~IOO
a..
LLJ
Q
150
200
Fig. 20.
DTPA- MANGANESE
(ppm)
10 20
o
o
30
........tJ
--0---0-
-.6.- - - -6,-
..0...........0...
o
DTPA - IRON
(ppm)
10 20 30
£9"" .:.
:..~.. 57ppm
./""::"""0
......................
,
[j
o
DTPA-COPPER
(ppm)
1 2
3
NATURAL SOILS
OLD MINE SOILS
NEW MINE SOILS
Distribution of DTPA-extractable Zn, Fe, Mn, and Cu in
natural soils and mines oils.
59
-------
soils especially late in summer when surface horizons are dry thus slowing
ion uptake from the zone where Zn is concentrated. Munshower and Neuman
(1978) found that several range grasses growing on unmined soils near
Colstrip had Zn concentrations below the dietary requirement for cattle for-
age. Zinc concentration in grasses decreased from spring throu~h fall.
Safaya (1978) found a slight response to Zn on North Dakota minesoils when
adequate Nand P were added.
Iron: Extractable iron generally increases with decreasing pH. Iron
distribution in old minesoils and natural soils are nearly uniform with
depth which may be due in part to the nearly constant pH of these soils with
depth (Fig. 20). Iron concentration is near the lower limit suggested by
Follett and Lindsay (1970). Iron deficiency may also occur on these soils
since free lime is abundant at most depths.
The distribution of iron in new spoils is not explained by pH differ-
ences. Iron content is much higher than in other soils. The large increase
in extractable iron at 100 cm corresponds to a layer of silty material
texturally distinct from other horizons. This layer may have been derived
from material below the water table where low redox potential caused ferrous
(Fe+2) iron to be the dominant form. Ferrous iron is much more soluble than
the ferric (Fe+3) form which would account for the elevated concentration.
Ferrous iron tends to oxidize to the ferric form and precipitate as iron
oxides when in contact with the atmosphere. Bands of iron oxide paralleling
the silty layer (Fig. 21) suggest that diffusion of ferrous iron and oxidation
does occur in new minesoils .
Manganese: Available Mn tends to increase with organic matter
crease with increasing soil pH and lime content. Manganese content
spoils and natural soils tends to increase near the surface as does
20). Adequate Mn for plant growth is indicated, however.
and de-
of old
Zn (Fig.
Manganese like Fe is also strongly affected by changes in the redox
potential (Ponnamperuna, 1972). Manganese concentration shows a large
increase in the silty layer at 80-100 cm in new spoils much like iron. A
thin section of a siltstone fragment shows precipitation of opaque Mn02 along
fractures indicating that reduced Mn is oxidized when in contact with the
soil atmosphere (Fig. 22).
Copper: Available Cu increases with increasing clay content and total
Cu in soils. As a result, Cu concentration decreases near the soil surface
unlike Zn and Mn. Decreased Cu content near the surface of old spoils and
natural soils may be due to organic matter - copper complexes which make Cu
less available to plants (Fig. 20).
Copper content of new spoils has an erratic distribution with depth.
Copper availability may be more influenced by differences in Cu content of
parent materials, than by other soil properties like organic matter, or clay
content.
Lead: Lead content of all soils increased slightly near the surface sim-
ilar to Zn and Mn (Fig. 23). New minesoils had an erratic Pb distribution.
60
-------
00-
r]
!-~
Fig. 21.
Bands of iron staining parallel the low chroma sandstone fragment
in the center of the picture.
Nickel:
(Fig. 23).
The distribution of nickel was similar to lead in most soils
Cadmium: Cadmium content was uniform
Cadmium content increased near the surface
slightly higher in extractable Cd than old
with depth in minesoils (Fig. 23).
in natural soils. New spoils were
spoils or natural soils.
The distribution of extractable Zn, Fe, Mn, Cu, Pb, Ni, and Cd in old
minesoils was similar to natural soils. The variation in element concentra-
tion with depth in old spoils and natural soils could be explained by the
effects of pH, and organic matter on element availability. The extractable
elemental content of new spoils was more closely related to the nature of
the parent material. The previous location of material comprising new spoils
may be a factor explaining the variability of element distribution of these
soils. A silty layer which perhaps was derived from an aquifer had highest
levels of nearly all trace elements examined. The reduced form of many ele-
ments, especially Mn and Fe, are more mobile than the oxidized form. Differ-
ences in mobility, and the rate of oxidation of reduced ions may have an im-
portant influence on phytotoxicity and ground water quality in mined land.
If it is assumed that old spoils were initially variable in trace element
concentration, like new spoils are now, then less than 50, but more than 3
61
-------
Fig. 22.
Thin section of siltstone fragment showing manganese bands
(mangans) paralleling fractures.
years are required for the trace element distribution to resemble that of
natural soils.
Other evidence of transformations of trace elements was found in mine
soils which contained coal fragments. Many coal fragments were surrounded
by a prominent concentric layer of iron-stained soil 2 cm thick (Fig. 24).
The pH of affected coal fragments was 2.1, the interior of the iron-stained
layer was 2.5, the outside of the layer was 6.0, while the spoil matrix was
8.3 (Table A-28). Banding only developed around coal fragments which con-
tained pyrite. Apparently the pyrite is attacked by Thiobaccilus ferroxidans,
a microorganism which gains energy through oxidation of the iron and sulfur
in pyrite (Temple and Colmer, 1951, Temple and Delchamps, 1953). One of the
by-products of this process is H2S04 which dissociates to cause the low pH.
Because of the large amount of CaC03 in these minesoils , and the small amount
of pyrite, only a small volume of soil is affected by the low pH. It appears
that the first product of pyrite breakdown is a ferrous sulfate complex, be-
cause the iron is mobile enough to diffuse away from the pyrite. Finally,
the ferrous iron is oxidized to the ferric form which precipitates in the
distinctive red bands, paralleling the coal fragment. The sulfate produced
by this process combines with calcium to form gypsum crystals replacing the
pyrite. From examination of the iron staining in this section it appears
62
-------
- 50
e
u
-
:1:100
.....
a.
w
c 150
200
-
E 50
o
-
:1:
..... I GO
a.
w
c
150
200
Fig. 23.
o
o
DTPA-LEAD
(ppm)
05 1.0
1.5
o
o
DTPA- CADMIUM
(ppm)
0.1 0.2 0.3
-0----0-
-A- - - -6,-
...0.............0...
o
o
DTPA-NICKEL
(ppm)
02 0.4
0.6
NATURAL SOILS
OLD MINE SOILS
NEW MINE SOILS
Distribution of DTPA-extractable Pb, Ni, and Cd in
natural soils and minesoils.
63
-------
~
\
Fig. 24.
Coal fragment showing bands of iron-staining paralleling
fragment. White material around coal is gypsum.
that the iron-stained area is made up of several distinct bands. The number
of bands roughly corresponds to the number of years the coal fragment has
been exposed to weathering. Thus, one band may be produced each year, for
example in late spring when the soil is wet and warm enough for biological
activity.
The process of iron-band formation around coal fragments is similar to
many transformations involving trace elements in minesoils. The mining
process can intimately mix materials from different segments of the over-
burden. As a result, the elemental content of the minesoil is often ini-
tially quite variable on a micro-scale « 10 cm). Iron and manganese have
been observed to diffuse away from zones of localized concentration (Figs.
22 and 24). This diffusion process acting through time should tend to homo-
genize the distribution of some trace elements. This process of homogeniza-
tion is unlike processes which have been observed in natural soils. In fact,
the opposite process often occurs. Natural soils are usually homogenous in
Mn and Fe content initially. Extreme weathering or periodic changes in redox
often cause localized concentrations or concretions of Fe and Mn to form.
Thus the unique origin of minesoils has resulted in unique processes of soil
development at least in the case of iron and manganese movement.
64
-------
Clay Mineralogy
The abundance of individual clay mineral species of selected horizons
was determined semi-quantitatively by x-ray diffraction methods. The three
groups of soils; old spoils, new spoils, and natural soils represent three
distinct mineralogic regimes. Natural soils formed in the top two meters of
geologic material and have been exposed to weathering for several thousand
years. Old spoils were derived from the upper 8 m of overburden, thus have
undergone less severe weathering. New spoils originated from materials
throughout the overburden perhaps with most material from just above the coal
seam. As a result of these different origins of material, three distinct
suites of clay minerals have resulted in these soils.
The clay fractions of three groups of soils had nearly equal proportions
of mica, smectite, and quartz (Table 9). The amount of kaolinite varied from
only moderate in natural soils to dominant in new spoils. Kaolinite abun-
dance increased as the depth from which the parent material was derived in-
creased. In other words, kaolinite would be expected to increase with depth
in the overburden. This agrees with the findings of Klages (1975) in his
analysis of several overburden cores from the Decker, Montana area.
Table 9. Clay mineral abundance in the clay fraction
and minesoils at Colstrip, Montana (values
mean from all horizons).
Clay mineral
Species
of natural soils
reported are the
Natural Soils
Old Mine Soils
New Mine Soils
Kaolinite
Mica
Smectite
Quartz
Calcite
Chlorite
Smec tite/ Chlor .
Vermiculite
3*
2
1
1
o
o
1
o
4
2
o
1
1
o
2
o
5
2
1
1
o
2
o
1
* 5
4
3
2
1
o
Dominant
Abundant
Moderate
Small
Trace
Not Detected
Clay-sized calcite is nearly absent in new minesoils. New minesoils
lack clay-sized calcite despite an abundance of carbonate in the whole soil.
Apparently the primary calcite grains are dominantly silt or sand-sized.
Natural soils are free of clay-sized calcite in the upper 50 cm due to com-
plete removal of calcite from these horizons. Old minesoils have a trace of
clay-sized calcite which may indicate that much of the silt- and sand-sized
carbonate has dissolved and reprecipitated in a 50-year period. Thin sections
65
-------
of old minesoils verifies this conclusion (Fig. 18).
Chlorite occurs in small amounts in new minesoils but not in other
soils. A similar smectite-chlorite interstratified mineral occurs in small
amounts in old minesoils. Removal of alternate brucite sheets from the
chlorite in new minesoils could have given rise to the interstratified min-
eral in old spoils. However, for this change to occur in 50 years, the chlor-
ite mineral would have to be very unstable in the chemical regime of these
soils.
Fabric-Related Properties
Clay: Natural soils generally contain more clay than mines oils indi-
cating a difference in parent material (Fig. 25). Old minesoils are sandy
because they were derived from partly resistant sandstone knolls. New spoils
are low in clay because of the dominance of silt and fine sand in the over-
burden, and the selective placement of sandy material in the upper two m of
the soil.
The bulge in clay content at 80 to 100 em in the new spoils corresponds
to a stratification of clayey material deposited by a scraper in the 1975-11
pedone Where scrapers are used to deposit minesoils, many abrupt changes in
texture are observed. Abrupt textural changes have a strong influence on
water and solute movement in soils. Sandy substrata can prevent percolation
of water until surface horizons are saturated (Gardner, 1968). Clayey sub-
strata may slow percolation and reduce infiltration rates. Abrupt changes
in texture influence soil management enough to be recognized in soil classi-
fication (Soil Survey Staff, 1975). In addition clayey substrata can be
strongly compacted if deposited when moderately wet. Severe compaction has
been observed to prevent root penetration in many new mine soils. A restrict-
ed rooting depth results in less available water for plant growth during the
critical mid-summer periods.
Clay is a mobile component in many soils. Removal of clay from the upper
profile and accumulation in B horizons, results in the formation of an argil-
lic horizon. An argillic horizon has formed in the Ethridge-4 soil between
10 and 31 em. Evidence of clay movement exists in the Boxwell-2 pedon (Fig.
26), but not enough has moved to form an argillic horizon.
As a result of higher organic matter and clay content, natural soils
have a much higher cation exchange capacity (CEC) than minesoils. CEC in-
fluences the quantity of exchangeable ions and, thus, affects soil fertility.
The average CEC for natural soils was 8 meq/l00 g while old, and new mine
soils averaged 5 and 3 meq/l00 g. The dominant clay minerals in natural
soils have slightly greater cation retention as evidenced by the higher CEC/
clay ratio.
Soil structure: Aggregation of primary soil particles into larger units
is soil structure. The basic soil structural unit is the ped (Brewer, 1976).
Formation of soil peds is favored by increasing clay and organic matter con-
tent (McHenry and Russell, 1943). In clayey soils, blocky structure develops
rapidly in the subsoil. Prismatic structure develops in sandier soils (White,
66
-------
- 50
E
o
-
:I:
r-
0-
W 100
C
Fig. 25.
CLAY (Ok)
o
20
30
40
50
60
10
o
150
SYMBOL SOIL TYPE
I~~~~~~~~~d "NATIVE"SOILS
ITIIIIJJ] OL 0 SPOILS
~ NEW SPOILS
Range in clay content for natural soils and minesoils .
1967). The arrangement of soil particles into larger peds decreases erodibil-
ity and increases pore space and thus infiltration. Formation of soil struc-
ture is, therefore, an important property affecting erosion and water
movement.
Minesoils differ markedly from natural soils in the distinctness
and kind of structural aggregates (Figs. 27 and 28). Most natural soils have
moderate granular structure in the A horizon. Natural soils are massive
below 130 cm where wetting and drying is infrequent and the weight of over-
laying soil prevents formation of peds.
Weak platy and granular structure has formed in the upper 50 cm of
many older minesoils. The platy structure may have resulted from compaction
by heavy vehicle traffic. Granular structure is most prominent in association
with the root systems of perennial grasses (Fig. 29). The relative strength
or prominence of peds increases with increasing soil age indicating that
67
-------
(~.' :;-~--.~.
\,.' ". .
, . ,. ...' I>
.,;11 ,"":- ..'..
~.~. #
. . y. .
/~. . ...
.: . ~ ,. . - . '.(
? ,
.. ;.,;.
... '.
L ~.
N/COLSi IO./~~~.
.SJ_\~ ..
Fig. 26.
Oriented clay (argillans) around sand grains of Boxwell B
horizons.
structure begins to form in minesoils within 50 years. New minesoils with
"topsoil" applied at the surface did not have granular structure which is
cornmon in A horizons of natural soils. Th~ topsoil salvaging and replacement
process destroys soil structure.
Some old spoils high in clay which were regraded in 1969 had vessi-
cular structure in the upper 5 cm. Where slow infiltration causes the top
few centimeters of soil to become saturated with water, air from lower in the
soil is entrapped in the surface layer and forms spherical voids which cause
vesicular structure when the surface dries to form a crust.
Bulk density: Old mines oils are nearly equal in bulk density to
natural soils, but new mines oils have higher bulk density (Fig. 30).
Density of mine spoils is related closely to the type of equipment used in
regrading spoils as well as to soil texture and natural processes that mix or
loosen soils.
Old spoils were deposited by side-dumping haul trucks. Materials
were deposited at their angle of repose as platforms were built outward from
a slope (Fig. 11). Many old spoils were compacted in the upper 30 cm due to
repeated vehicle traffic; while below this depth they have low bulk density.
The top 5 to 10 cm of old minesoils have decreased in bulk density due to
68
-------
STRUCTURE
KIND
MAS.
o
PL.
GR.
BLK.
COL.
50
................
................
.................
..".'.""...'"
.................
..................
.....................................
.....................................
.....................................
.....................................
"..'...'..'.""..".......'.....'..
.....................................
,...".,...,..".,.""...""."",.
............................,........
-
E
o
-
.....................................
...'.'.'.".""'.""'.""".'..'..
:I:
t-
a..
w 100
C
'...""'.".."'."."..."'."'..'.
.....................................
......................................
"""""""""""""""'.".'"
......................................
"".""""".""""""""""'"
.......................................
.""""."'.""""""""""""'.
.........................................
..........................................
...........................................
............................................
..............................................
................................................
..................................................
[[[
[[[
[[[
."""""""""""""""""""""""""""
[[[
[[[
[[[
[[[
[[[
"'.""""'."""""""""""""""""""".
[[[
[[[
[[[
[[[
[[[
[[[
[[[
[[[
[[[
[[[
""""""""""""""""""""""""'"
......................,...........................
.......................,.........................
.......................,.........................
................................................
...............................................
.........,....................................
............................................
....,......................................
................,........................
"""""""""""""""'."""'"
SYMBOL
r~~~~~~~~~~~t
[I]]IJ]
~
SOIL TYPE
"NATIVE" SOILS
150
OLD SPOILS
NEW SPOILS
Fig. 27.
Range in kinds of structure in natural soils and minesoils.
-------
STRUCTURE
GRADE
MAS.
o
V.WK
WK.
WK.-MOD. MOD. MOD.~ ST. ST.
50
-
E
(,)
-
:I:
J- 100
a.
W
£:)
. . . . .....,.
o . . . . . . ..
. . . . .
. . . . .
. . . . .
. . . .
. . . .
. . . .
. . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
. . . . . .
, . . . . .
I . . . . .
. . . . .
. . . .
150
SYMBOL SOIL TYPE
I; ~; ~ ~ ~ ~ ~ ~ d "NATIVE"SOILS
ITIIIIIIl] OLD SPOILS
~ NEW SPOILS
Fig. 28.
Range in structure grade in natural soils andminesoils .
Unconsolidated rock fragments are unlike other rock fragments in that
they hold a significant amount of plant-available water. Water is apparently
withdrawn from fragments by plants during the growing season. Roots cannot
penetrate into the fragments, however. Soft rock fragments respond in part
like rock, and in part like soil. They are similar to materials which under-
lie paralithic contacts in local soils.
Soft rock fragments weather at a rapid rate in the upper layers of mine
soils (Fig. 32). Rai and others (1974), in New Mexico and Grandt and Lang
(1958) in Illinois found that shales weathered rapidly to create a clayey
layer at the surface of spoils. The fine-textured crust increased run-off
and was a limitation to reclamation. Rock fragments were weathered in the
upper 20 cm of minesoils after 50 years in this study (Fig. 33). Soft sand-
stone appears to weather more rapidly than siltstone fragments. Porcelainite
fragments are resistant to weathering as are indurated sandstone fragments.
Coal does not disintegrate like other rock fragments, but may oxidize into
leonardite-like material after exposure to' weathering.
70
-------
Fig. 29.
c3
.::>'"
T f
-'6
....s
.. t-
'0
""~
CD CD
'0
'" '"
'0 .
CD CD
- '0
!!'.~
"'0
00
Granular structure in old minesoils is associated
with the root systems of perennial grasses.
Cycles of wetting, and drying; and freezing, and thawing; or mechanical
disruption by roots may cause rock fragment weathering (Fig. 34). Workers at
the University of Wyoming devised artifical weathering tests to evaluate the
stability of rock fragments from overburden (Univ. of Wyo., 1976).
Thin sections of rock fragments from various depths were prepared to
investigate the mode of rock weathering. Nearly unweathered fragments from
lO~ cm in 50-year old minesoils contain very little cement, so that simple
grain-packing and compaction provides the only cohesiveness. Freezing and
thawing, mechanical disturbance by roots, or expansion of clay minerals might
provide sufficient energy to disintegrate fragments. Rapid wetting of frag-
ments which entraps air causes fragments to slake in a few seconds or minutes.
-
71
-------
BULK DENSITY
(g/cm3)
1.1
1.2
1.3
1.4
1.5
1.6
1.7
1.8
o
50
-
E
SIOO
x
....
0-
W
C
150
SYMBOL SOIL TYPE
I~~~~~~g~~~~ "NATIVE"SOILS
ITIIIIIIll OLD SPOILS
~ NEW SPOILS
Fig. 30. Range in bulk density for natural soils and minesoils .
72
-------
. I
.;;.'
Fig. 31.
Scrapers (left) and bulldozers (right) create minesoils
with different bulk densities.
Nearly unweathered fragments from 100 cm contained approximately 10% calcite
sand grains by volume. Weathered rock fragments from 20 cm in all minesoils
contained fewer calcite grains. In weathered fragments, CaC03 is instead
dispersed throughout the fragment as grain coatings of reprecipitated CaC03
(Fig. 35). Dissolution of 10% of the sand grains in the fragment could have
caused disintegration. Further research on the role of rock fragments in
minesoils is needed to evaluate their effect on plant growth.
Orphan Spoils
Hany ungraded spoil ridges or "orphan spoils" are common in the Colstrip
area. These steep spoils consist primarily of clayey materials from the pit
bottom and are unlike the flattened platforms of excess overburden commonly
referred to as old spoils throughout this report.
The vegetative cover on orphan spoils with similar slope and aspect vIas
found to vary from 0 to nearly 100%. Cover was observed to decrease abruptly
over a few feet of distance. A curious dark greasy-looking crust was observed
on some non-vegetated areas (Figure 36). Several soil samples were collected
from orphan spoils to see if soil properties would explain the lack of vege-
tation on some areas (Table 10).
Orphan spoils which supported vegetation were fairly similar to other
mine soils in the Colstrip area. Non-vegetated spoils, however, had a much
lower pH and higher EC than any other materials encountered in the area.
Extractable levels of trace elements were similar to vegetated orphan spoils.
Non-vegetated crusted spoils had extremely low pH (2.3 to 2.7) and EC greater
than 15 mmhos/cm. Visible soluble salt crystals at the surface were probably
magnesium sulfate. Hagnesium content of a saturation extract generally
exceeded 2000 ppm. Elevated levels of Hn, Zn, and Ni were found in crusted
73
-------
, -
~!- .~-
Fig. 32.
A single shale fragment is shown to weather
more quickly near the soil surface in this
four-year-old mines oil. .
74
-------
Fig. 33.
OLD
MINE
o
o
1928-9
ROCK FRAGMENT VOLUME ('1e)
10 20 30 40 50
60
10
- 20
E
2
J:
t 30
'"
Q
40
50
NEW MINE SOILS
o
o
1970-15
ROCK FRAGMENT VOLUME C'1e)
10 20 30 40 50 60
10
- 20
E
2
J:
t 30
'"
Q
40
50
LEGEND
SOILS
o
o
1929-10
ROCK FRAGMENT VOLUME C'1e)
10 20 30 40 50
60
10
- 20
E
2
J:
t 30
'"
Q
40
50
lithologic
,/ dlscontmuity
I
o
o
1975-11
ROCK FRAGMENT VOLUME ('1e)
10 20 30 40 50
60
10
- 20
E
2
J:
t 30
'"
Q
40
50
SCORIA
~
D
SHALE
SOFT SANDSTONE
Rock fragment content of minesoils
varying in age.
75
lithologic
dlscontlnU'IYl\
-------
F~.
34.
Photo of 1928 mines oil showing that
weathered in the upper 20 crn but are
depth.
rock fragments have
cornman below that
76
-------
" i-'~;
\' I.- ..'
Fig. 35.
Thin sections taken within unweathered (above) and weathered
(below) sandstone fragments. CaC03 occurs in discrete grains in
unweathered fragments but is dispersed in the weathered state.
77
-------
'~ ..... .:-'
.~. ~ L.~
.'" ' " . j..11 ...t~
., ~.~~~. "~.. "'."'T..~"
'V ~- . . . . ... -,. III
;. ...;~~. ';...\.~~
:\ .v~:... .'~.~
',,' ~ '~"ut"'.'
J ' ".:,.
. --...
.~. - I t"!- .. . -~ ..._~
.:, . ~....... -- . ~"-1
".....-. ...
¥,~'- ---.....--.i
... Jf. ~- .....
u.-::' ~"
" ...
......
Oil
° .
Fig. 36.
Vegetated, non-vegetated, and crusted areas occur in close
proximity on orphan spoils.
78
-------
Table 10. Selected soil analyses from vegetated, non-vegetated, and non-
vegetated, crusted orphan spoils in the Colstrip, Montana area.
Saturation
Extract DTPA Extract
Depth EC Mg Ca Na Mn Cu 2n Pb Cd Ni Fe
(cm) pH (mmhos/cm) mg/1 Ug/g
VEGETATED 0-2 5.6 .4 18.3 31.8 3.6 35.0 5.53 11. 40 0.20 0.06 2.64 179
2-5 7.3 .5 16.3 58.5 3.2 18.3 1.88 2.00 1.40 0.07 0.86 10.5
5-10 8.3 .3 10.0 37.0 2.4 11.5 1.74 1.16 1.24 0.05 0.78 6.9
NON-VEGETATED 0-2 3.9 1.4 67.5 95.4 8.1 38.9 5.36 9.40 0.14 0.06 3.02 210
2-5 4.1 .9 49.6 67.2 4.2 39.2 3.55 8.10 0.14 0.12 3.20 172
5-10 7.6 .8 31. 7 84.5 3.3 24.4 2.12 3.30 2.00 0.10 0.88 15.7
NON-VEGETATED 0-2 2.7 >15.0 2620 63.8 2.0 103.6 3.55 18.84 0.36 0.10 5.20 715
CRUSTED
2-5 2.3 >15.0 2880 54.5 1.2 86.9 2.02 18.80 0.40 0.11 5.50 1100
5-10 2.3 >15.0 1333 81.0 2.1 61.0 1.67 13.84 0.36 0.08 3.10 831
non-vegetated spoils. Manganese andNi concentrations exceeded levels sus-
pected of causing phytotoxicity CMDSL, 1977).
The low pH in orphan spoils probably resulted from the oxidation of
pyrite which is often concentrated in the upper few feet of the coal seam.
Because of a lack of sufficient water to leach the spoil, salts accumulated
as products of pyrite oxidation. At the low pH in these spoils, it is
possible that some clay minerals or other silicate minerals were rapidly
weathered to produce the high Mg content of the spoils. Sulfate is a direct
product of pyrite (FeS2) oxidation. The dark crust results from the presence
of free sulfuric acid which combines hygroscopically with water causing the
soil surface to remain wet. Salts associated with a similar crust which
forms in minesoilsi of the eastern US (Fanning and others, 1977) included
halotrichite (FeA12 (S04)4 . 22H20) and kalinite (KAl(S04)2 . llH20).
It is often assumed that high sulfur content in conjunction with high
precipitation causes the low pH which forms in eastern spoils. Formation of
acid spoils in this climate, however, suggests that the acid-base balance in
the overburden may be more important than precipitation in acid formation
(Smith and others, 1976). Caruccio (1978), and Arora and others (1978)
report that pyrite morphology also influences acid-producing potential. The
high calcium carbonate content of spoils in the West apparently provides
enough buffering capacity to prevent acid-formation except when large amounts
of pyritic coal is mixed with the overburden.
79
-------
SECTION 8
WATER RELATIONS
Availability of soil water for plant growth is a major limitation to
Western reclamation (Hodder, 1978). Precipitation is a primary factor influ-
encing the amount of soil water in western minesoils. Soils with low
infiltration rates will not absorb precipitation during high intensity storms
or snowmelt. Run-off from these types of soils can result in severe erosion
especially on unvegetated sites.
Once water enters the soil, its movement is governed by water potential
gradients. Water potential is a measure of the energy state of water in
soil. It is influenced by gravity, salt content, matric potential, and
other factors. In a saturated soil, water moves downward to the water table
under the influence of gravity. Mine soils in the West are seldom, if ever,
saturated. In these soils, water moves by unsaturated flow which can be
upward, downward, or lateral in direction. Water moves from zones which
have a high water potential to those with lower potentials. In unsaturated
soils, this means that water moves to zones that are drier or higher in salt
than the surrounding soil. As plant roots extract water from soil, a water
potential gradient is produced which causes water from other soil zones to
flow toward the root. The rate of flow especially in dry soils is very
slow. As a result, roots can extract a substantial amount of water only
from a soil volume several cm in diameter. Therefore, compacted soil
horizons which impede deep penetration of roots may severely limit the water
available to the plant. Likewise, a young plant community without a well-
developed root system probably has less water available to it for growth.
In this study, the water movement patterns in old, and new minesoils ;
and natural soils have been observed. Differences in water movement were
related to soil physical properties and root distribution to evaluate how
minesoils differ from natural soils hydrologically.
Infiltration
Infiltration rates on all soils studied varied from 6 to 15 cm/hr
(Table 11, Appendix B). There were no significant differences between infil-
tration rates on undisturbed soils and minesoils. Differences in infiltra-
tion rates between individual sites were highly correlated with surface sand
content (r = .85) and silt content (r = -.84).
Infiltration into minesoils was not slower than into natural soils as
has been shown by other studies in the region (Gilley and others, 1977b;
Dollhopf and others, 1977; Arnold, 1977; Miyamoto, 1977). Moderately rapid
infiltration rates (Soil Survey Staff, 1951) can apparently be attained
80
-------
Table 11.
Infiltration rate after 30 minutes on natural soils and
of the Colstrip, Montana area. Reported values are the
three replicates.
minesoils
mean of
SITE
SOIL TYPE
-1
INFILTRATION (cm hr ) *
1975-11
Ethridge-4
1929-10
Boxwel1-2
1928-9
1928-7
1973-12
Chinook-8
Riedel-6
1970-15
1972-13
new spoil
natural spoil
old spoil
natural soil
old spoil
old spoil
new spoil
natural spoil
natural spoil
new spoil
new spoil
5.93 a
8.20 b
8.90 b
10.63 c
11.83 d
12.43 d
14.00 e
14.23 ef
14.87 ef
14.87 ef
15.30 f
* numbers followed by the same letter are not significantly different at
p < .05.
quickly on minesoils by using non-sodic, coarse-textured surface materials.
The presence of impermeable subsoil layers would be expected to eventually
decrease infiltration rates (Gilley and others, 1977b).
Even though infiltration is moderately rapid on Colstr1p minesoils ,
erosion is still common in the mine area. Fine and very fine sand, which is
dominant in these soils, is easily entrained by running water. Therefore a
small amount of run-off occurring as a result of high intensity storms can
cause severe erosion. Rapid establishment of vegetation is mandatory for
erosion control even on minesoils with moderately rapid infiltration.
Water Flow Patterns
Precipitation patterns during 1976 and 1977 allowed the s01ls to be
observed under two climatically different years. A wet spring and dry summer
occurred in 1976 with precipitation 111% and 30% of normal for the two
periods. In 1977, a dry spring (62% of normal) was followed by a wet summer
(146% of normal, Fig. 37).
A similar general pattern of water use occurred in all soils. Maximum
water content was observed in April after snowmelt and initiation of spring
rains. Most of the profiles were recharged with water to at least two
meters. As soil temperature increased, water was withdrawn from the shallow-
est soil depths by growing plants. As water in surface horizons was deplet-
ed, the zone of maximum water use shifted to progressively deeper depths. By
late summer soils were at their driest; plant-available water was depleted
from much of the root zone. Little change in water content occurred during
most of the fall and winter. Only a small amount of recharge occurred in the
upper 30 to 50 cm during this period. During the coldest winter months,
water content was observed to increase in the upper 50 cm and again decrease
by early spring. This phenomenon has been noted in other frozen solIs in the
81
-------
Fig. 37.
4 1941 - 1970 10
AVERAGE 8
3
6
2
4
1 2
0 0
(/)
4 1976 10 ffi
3 8 .....
a&J
6 2
2 -
4 .....
1 z
2 a&J
o 0 ()
(/)
a&J
:I:
()
Z
I
Z
o
.....
~
-
Q.
-
()
iLl
a::
Q..
. 1977
-
l-- ~ I
. ,
4
3
2
I
o J
N
F
M
A
M
J J A
MONTH
o
5
Average monthly precipitation is shown in comparison to 1976
and 1977 totals.
82
D
10
8
6
4
2
o
-------
Northern Great Plains and has been related to water vapor movement in
response to temperature gradients (Ferguson and others, 1964; Willis and
others, 1964).
Although the general pattern of water movement was similar in all soils,
the magnitude of recharge, stored soil water, water use, and the timing of
these events differed in old and new minesoils, and natural soils. For
example, in Fig. 38 the stored soil water in the upper 150 cm of the soils is
shown as a percentage of the maximum recharged level observed early in 1976.
Approximately 50% of the stored soil water should be available for plant
growth. It is apparent that water is used more rapidly from minesoils than
natural soils during the summer of 1976. The rate of water use in new mine
soils declines by mid-summer so the total depletion is similar to natural
soils. Depletion continues in old minesoils, however, until nearly all
available water is withdrawn from the upper 150 em. As a result of these
water removal patterns, only limited recharge occurred in old minesoils
during the dry spring of 1977. Thus less total water was available in the
drier year. New minesoils were also recharged slightly less than natural
soils.
Differences in water use are probably largely a result of differences in
plant communities. Natural soils support a mixture of cool- and warm-season
native grasses, with some forbs and shrubs; which use water very conserva-
tively. Water removal begins more slowly in the spring when use by intro-
duced species on new minesoils is rapid. Water use in natural soils
continues through the summer by warm-season grasses, forbs, and shrubs. New
minesoils are dominated by introduced perennial grasses with some introduced
shrubs. These grasses such as Bpomus inermis~ Agpopypon apistatum~ and
A. eZongatum are characterized by early growth. As a result, water is used
rapidly in the spring but decreases to near zero by mid-summer when these
species enter summer dormancy. Old minesoils are dominated by shrubs, half-
shrubs, and annual grasses. This plant community tends to withdraw water
early in the spring, but continues to remove water throughout the growing
season. By late summer, nearly all plant available water is withdrawn from
the upper 150 cm. Only deep-rooted shrubs are adapted to growing in these
conditions. As a result of this nearly complete use of soil-water in a
wetter-than-normal year, only partial recharge of soil water occurred in
1977. a dry year. Community production would be expected to be most variable
and unstable on old minesoils due to the water use patterns. Plant communi-
ties on natural soils which use water more conservatively would be expected
to have lower productivity in a wet year than plant communities on mine
soils, but higher than minesoils in a dry year because more complete
recharge would occur.
Observation
with more detail
are shown to aid
of water content by depth shows the dynamics of water use
(Figures 39-53). Bulk density and root biomass of the soils
in the understanding of water distribution patterns.
During May and June, water is used from the upper 50 cm of natural soils
where the soil is warmest and roots most abundant. The zone of maximum water
use shifts downward to 100 cm by mid-summer. Late 1n the summer only a small
amount of available water is left in the upper 50 cm, however, only small
83
-------
I-~
Zz
W::J
I- ~ 100
Z- ~ a:: 60
l.L..
~o 50
-~
80 40 J J A S 0 N 0 I J F M J J A
19761 1977
'Fig. 38.
Profile water content (em in upper 150 em) is shown as a percentage of the recharged
content in June, 1976. The line at 50% represents the approximate wilting point.
-------
50
100
E
u
J:
I- 150
Cl.
w
a
200
250
E 100
..8
J:
I-
~ 150
a
o
10
SOIL WATER
20 30 40
. . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . .
CHINOOK - I
CONTENT
o 10
LEGEND
DATE POTENTIAL DATE
o 619/76 ~ > 15 BARS 0 1/15/77
t:,. 7/11/76 C=:J 0.1-15 BARS t:,. 2112177
o B/Ii/76 !:::}}:;:J 0 - 0 1 BARS 0 4/3/77
o 11124/76 ~':':':':':':'3 <0 BARS 0 4/15/77
-...-.-...-.-
8
BULK
10
o
50
200
250
Fig.
DENSITY
12 14
(g/cm3)
16
. 5129/77
... 7/31/77
180
ROOT BIOMASS (g/m3)
I 0 2.0 3.0 4.0
39.
Seasonal water content, bulk density,
root biomass for the Chinook-l soil.
85
and
-------
BOXWELL - 2
o
20
1976
SOIL WATER CONTENT (%)
30 40 0 10 20
1977
40
10
50
100
E
u
:I:
I- 150
a.
IJJ
o
: :;:::::;
i t~\.
:I~
200
250
30
.'/:::!::>::t
::
LEGEND
DATE POTENTIAL DATE
o 619/76 ~ > I!! BARS
~ 7/11/76 CJ 0 I-I!! BARS 6. 2/12/77
[2]]
0 B/II/76 ::::::::::!:: 0-01 BARS 0 4/3/77
o 11/24/76 E:::::::::::::3 <0 BARS 0 4/1!!/77
. 5/29/77
. 7/31/77
8
o
BULK DENSITY (g/cm3)
10 12 1.4 16
50
E 100
S
:I:
I-
~ 150
0 )
200
250
Fig. 40.
180
ROOT BIOMASS (g/m3)
10 2.0 3.0 40
Seasonal water content, bulk density, and
root biomass for the Boxwell-2 soil.
86
-------
E
...
:I:
~ 150
UJ
o
E 100
~ .
:I:
~
fu 150
o
o
1948-3
SOIL WATER CONTENT (%)
30 40 0 10 20
40
10
20
1976
30
1977
50
100
200
250
LEGEND
DATE POTENTIAL DATE
~ > 15 BARS 0 1/15/77
t:. 7/11176 C:=J 0 1-15 BARS t:. 2112177
o B/II/76 k/;};:I 0 - 0 I BARS 0 4/3/77
o 11/24/76 ~;:;:;::::::;:j <0 BARS 0 4/15177
".""
. 5/29/77
A 7/31/77
.8
o
BULK DENSITY (g/cm3)
I~ 1.2 1.4 1.6
ROOT BIOMASS (g/m3)
1.0 20 30 4.0
1.80
50
200
250
Fig. 41.
Seasonal water content, bulk density, and
root biomass for the 1948-3 8011.
87
-------
E
u
I
t- 150
ll.
w
o
E 100
~
I
t-
~ 150
o
Fig. 42.
ETHRIDGE - 4
SOIL WATER CONTENT ("10)
30 40 0 10 20
77
o
10
50
..
100
200
250
DATE
LEGEND
POTENTIAL
o &'9/76
6. 7/11/76
o B/II/76
o 11/24/76
~
CJ
1::::::::::::::1
~:;:;:;:;:;:.:~
-.-.-.-.-.-:.
0-0 I BARS
<0 BARS
> 15 BARS
01-15 BARS
8
o
BULK DENSITY (g/cm3)
10 12 14 1.6
1.80
50
200
250
30
40
DATE
6. 2/12177
o 4/3/77
o 4/15/77
. 5/29/77
... 7/31/77
ROOT BIOMASS (g/m3)
1.0 2.0 3.0 4.0
Seasonal water content, bulk density, and
root biomass for the Ethridge-4 soil.
88
-------
E
u
I
h: 150
w
o
E 100
3
I
t--
~ 150
o
1928-5
SOIL WATER CONTENT (%)
30 40 0 10 20
197
50
o
10
100
200
250
30
40
LEGE N D
DATE POTENTIAL DATE
o G/9/76 ~ > /5 BARS 0 1/15n7
t::,. 7/11/76 c=J 01-15 BARS t::,. 2/12/77
o B/II/76 L«] 0 - 0 I BARS 0 4/3/77
o 11/24/76 ~:::::::::::::~ <0 BARS 0 4/15/77
. 5/29/77
.8
o
BULK DENSITY (g/cm3)
1.0 1.2 14 1.6
50
200
250
180
ROOT BIOMASS (g/m3)
10 2.0 30 40
Fig. 43.
Seasonal water content, bulk density, and
root biomass for the 1928-5 80i1.
89
-------
o
RIEDEL - 6
SOIL WATER CONTENT
20 30 40 0 10
(8/.)
20
40
10
50
100
E
~
J:
~ 150
Il.
Lo.I
0
200
250
LEGEND
DATE POTENTIAL DATE
o &'9/76 ~ > I~ BARS 0 1/1~/77
~ 7/11/76 CJ O.I-I~ BARS ~ 2112/77
[J B/II/76 1:::<::::::::1 0-0.1 BARS [J 4/3/77
o 11/24/76 I:::::::::~:::I <0 BARS 0 4/1~/77
. ~129/77
BULK DENSITY (g/cm3) ROOT BIOMASS (g/m3)
.8 1.0 1.2 14 1.6 180 1.0 2.0 3.0 4.0
0 ~
50
E 100
...!:!
J:
~
fu 150
0
200
250
Fig. 44. Seasonal water content, bulk density, and
root biomass fo~ the Riedel-6 soil.
90
-------
E
u
J:
~ 150
a.
w
o
E 100
...!:! .
J:
~
PJ 150
o
Fig. 45.
1928-7
SOIL WATER CONTENT
20 30 40 0 10
. ......' .
......,..........
o
10
50
100
200
250
("10)
20 30 40
....,..' ""....
. ................
~
LEGE N D
DATE POTENTIAL DATE
o 619/76 ~ > 15 BARS 0 1/15/77
t:. 7/11/76 c=J 0 1-15 BARS A 2/12/77
o 8/11/76 F;:::;:;:
-------
o
10
20
SOIL
30
WATER
40
CHINOOK- 8
CONTENT
o 10
50
100
E
u
J:
f- 150
a.
w
0
200
250
DATE
o &'9/76
A 7/11/76
o 8/11/76
o 11/24/76
.8
BULK
10
o
50
E 100
oS
J:
f-
~ 150
o
200
250
LEGEND
POTENTIAL DATE
~ > 15 8ARS 0 1/15/77
CJ 0.1-15 BARS A 2/12177
V::::;:;:J 0-01 BARS 0 4/3/77
~::~:::::;:;:j <0 BARS 0 4/15/77
. 5/29/77
180
ROOT BIOMASS (g/m3)
10 2.0 3.0 4.0
DENSITY
12 14
(g/cm3 )
16
Fig.
46.
Seasonal water content, bulk density,
root biomass for the Chinook-8 soil.
92
40
and
-------
50
100
E
u
I
I- 150
a.
w
0
200
250
E 100
3
I
I-
~ 150
o
o
50
200
250
Fig.
o
20
SOIL
30
1928-9
WATER CONTENT
40 0 10
10
LEGEND
DATE POTENTIAL DATE
o &'9/76 ~ > 15 BARS 0 1/15/77
/:" 7/11/76 CJ 0.1-15 BARS /:" 2/12/77
o 8/11/76 I»:}:j 0-0 I BARS 0 4/3/77
o 11/24/76 E:;:;:;:;;:;;;i <0 BARS 0 4/15/77
.8
BULK
10
(g/cm3)
16
DENSITY
12 14
47.
. 5/29/77
("10)
20
30
. . ..... ..
1977 ::::::::::::::::::::::::::::::
...............
........,..,...
.........,.....
...............
. . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . .
. -,........
. ',' ..',',',',',',',',',.
,.:-'.-:: .-::::;:::::::::::::.:
.,' . ,',',',',',',',',' .0.
o .. ......... .
. ,', ,',',',',',',',',' .°0"
o. .............
. ',',',',',',',',',' '"0°,
" ',',',',',',',',',' ",'0"
. ........... ...
0'" ,',',',',',',',',',',', ,',0.0
-,.......... ...
" ,',',',',',',',',',',','0","0"'
............ ...
,',',',',',',',',',',',',' ""'"0"
',',',',',',',',',',',',',' ",".".'
",'.......". ....
,',',',',','.',',',','.',', ......,
,'.',',',','.',',',',',',',........
"".".,.", ....
",.".""". .'.'
"".,.".". ....
..,."""",. ....
""".""., ....
"."" "". ....
,."". ",., ....
".,." ,.". ....
,."".""., ....
"""",.". ....
".""."., ....
"".""." ....
".".""" ....
"""."." .....
.,.".,."" ....
"..,."". .....
,'.,."."" ....
.,...."", .....
.,.,."."" ....
..",.".,. .....
.,.,."."" ....
"",."", .....
, , . , ~ , ' , , ' " ....
II
I
'7
180
ROOT BIOMASS (g/m3)
10 20 3.0 40
93
Seasonal water content, bulk density,
root biomass for the 1928-9 soil.
40
and
-------
50
100
E
u
:I:
~ 150
a..
UJ
o
200
250
50
E 100
S
:I:
~
~ 150
o
200
250
Fig. 48.
1929-10
SOIL WATER CONTENT ("10)
20 30 40 0 10 20
~i"
j.:..::!I!!1i:~!:.I:ii.:!!i:
r::)::::::::::::::::::U:::::
I;:::;:::;:::;:;:::::::;:::;:::;::
to',',',',',',',',',',',',',',',',
f::::::::::;::::::;:::::::::::::::
(::::::::::::::::::::::::::::::::::
.:;:;:;:;:;:;:;:;:;:;:;:;:::;:::;:;::
?!!!HH:!!:!!!!!!!!!!/!!!
o
10
30
40
.................
"""""""""
t-:-:';';':';';':';';':-:':';';':
;;:::::;:::::;:::;:;:::;:::::;:::
1::::::::::::::::::::::::::::::::::
.~....................~...........
LEGEND
DATE POTENTIAL DATE
o 619/76 ~ > 15 BARS 0 1/15/77
t:. 7/11/76 c=J 0.1-15 BARS t:. 2/12177
o B/II/76 1::::;:;:::;:::1 0- 01 BARS 0 4/3/77
o 11/24/76 ~:::::::::::::~ <0 BARS 0 4/15/77
. 5/29/77
.. 7/31/77
8
o
BULK DENSITY (g/cm3)
10 1.2 14 1.6
1.80
ROOT BIOMASS (g/m3)
1.0 2.0 3.0 4.0
Seasonal water content, bulk density, and
root biomass for the 1929-10 soil.
94
-------
E
u
J:
~ 150
LLJ
a
E 100
S
J:
t-
~ 150
a
F1g.
o
50
100
200
250
.8
o
50
200
250
10
1975-11
SOIL WATER CONTENT (%)
20 30 40 0 10 20
197i/~ 197
V:::::::;:: : :: :::::::~:
,,;,>;,:-:,;..,", .;.:-:.;.:
~::::::::::::. . .'::;:;:;:
~
LEGEND
DATE POTENTIAL DATE
o &9/76 ~ > 15 BARS 0 1/15/77
t:. 7/11/76 c=J 01-15 BARS t:. 2/12/77
o B/II/76 k::::::::j 0-01 BARS 0 4/3/77
o 11/24/76 f("'-r~";~ 0
.:.:.:.:...:. <0 BARS 4/15/77
. 5/29/77
A 7/31/77
30
40
,............
1,',',',',', ',',',',',',',
(::::::::: 0:::::::::::::
:...............
BULK DENSITY (g/cm3)
1.0 12 14 1.6
180
ROOT BIOMASS (g/m3)
1 0 20 30 40
49.
Seasonal water content, bulk density, and
root biomass for the 1975-11 s011.
95
-------
E
<.>
I
I- 150
Q.
IJJ
a
E 100
..8
I
I-
~ 150
a
o
50
100
200
250
.8
o
50
200
250
Fig. 50.
1973 - 12
SOIL WATER CONTENT ("10)
30 40 0 10 20
1977
10
20
1976
DATE
LEGEND
POTENTIAL
o &'9/76
t:. 7/11/76
o 8111/76
o 11/24/76
~
c=J
I}};:::;:I
miiJ... ..
.-.-.-.:,.-,
.-.-;,e..-,
0-01 BARS
<0 BARS
> 15 BARS
01-15 BARS
BULK DENSITY (g/cm3)
10 12 14 1.6
30
40
. . . . ,
...........,
.......,....
.........."
............
....,..,...
.........".
.".......,.
......,.....
...........
...,........
. . . . . . . . . . .
,...........
..,........,
. . . . . . . . . . . .
. . . . . . . . . . . .
...,........
.......,...
.,..........
....,.......
.........,..
",......."
....,.......
. . . . . . . . . . . .
............
....,.......
........,...
,..........,
............
.........',
.,..........
......,.....
. . . . . . . . . . . .
DATE
o 1/15/77
t:. 2/12/7 7
o 4/3/77
o 4/15/77
. 5/29/77
. 7/31/77
180
ROOT BIOMASS (g/m3)
10 2.0 3.0 4.0
Seasonal water content, bulk density, and
root biomass for the 1973-12 soil.
96
-------
E
u
J:
I-
a.
IJJ
a
E 100
S
J:
I-
~ 150
a
o
SOIL
30
WATER
40
10
20
50
100
150
200
250
DATE
o 619/76
t:. 7/11176
o 8/11176
o 11124/76
~
CJ
!;:::}:::l
~':-:':':':':;3
e.-.e.-.....-
8
BULK
10
(g/cm3)
16
DENSITY
12 14
o
50
200
250
Fig.
51.
Seasonal water content, bulk density,
root biomass for the 1972-13 soil.
1972-13
CONTENT
o 10
30
40
..
.....
...
.,-,
LEGE N D
POTENTIAL
DATE
> 15 8ARS
01-15 BARS
o 1/15177
t:. 2/12177
o 4/3/77
o 4/15/77
0-0 I BARS
<0 BARS
. 5/29177
10 7/31/77
180
ROOT BIOMASS (g/m3)
10 2.0 30 40
97
and
-------
E
u
J:
~ 150
UJ
o
E 100
..!::! .
J:
I-
~ 150
o
50
100
200
250
50
200
250
Fig. 52.
o
LEGEND
DATE POTENTIAL
o &'9176 ~ > 15 BARS
t::. 7/11/76 C=:J 01-15 BARS
o B/11176 1:::::::<::..:1 0-0.1 BARS
o 11/24/76 I::::::::::::::J <0 BARS
8
o
BULK DENSITY (g/cm3)
1.0 1.2 14 1.6
1969-14
CONTENT
o 10
180
DATE
o 1/15/77
l::. 2/12177
o 4/3/77
o 4/15/77
. 5/29177
.... 7/31/77
ROOT BIOMASS (g/m3)
1.0 2.0 3.0 4.0
Seasonal water content, bulk densitYI and
root biomass for the 1969-14 soil.
98
-------
o
50
100
E
u
::I:
b:: 150
w
o
200
250
.8
o
50
E 100
S
::I:
I-
~ 150
o
200
250
Fig. 53.
1970 - 15
10
WATER CONTENT (%)
40 0 10 20
40
DATE
o &'9/76
t:. 7/11/76
o 8/11/76
o 11/24176
~
CJ
t;:::;:;:;:;::J
t:::':;:;';';-j
-.-.-.-.-:.:-:
BULK DENSITY (g/cm3)
I~ 12 1.4 16
30
LEGEND
POTENTIAL
DATE
> 15 BARS
01-15 BARS
o 1/15177
t:. 2/12/77
o 4/3177
o 4/15/77
. 5/29/77
0-0.1 BARS
<0 BARS
A 7/31/77
180
ROOT BIOMASS (g/m3)
1.0 2.0 3.0 4.0
Seasonal water content, bulk density, and
root biomass for the 1970-15 soil.
99
-------
amounts of water have been used below 100 cm. Since roots extend beyond 100
cm, most plants have access to water even late in the growing season. Few
physical restrictions to water movement or root growth occur in natural soils
except in the Riedel-6 soil which hasaparalithic contact at 50 cm which
restricts root growth. On April 3, 1977 a large amount of water was observed
in the upper part of the profile. By mid-April the water had drained down-
ward as a wetting front. The depth of penetration of this front represents
the depth of recharge. In nearly all natural soils the wetting front moved
to 250 cm leaving the profile at field capacity. Some drainage may occur
below the root zone in natural soils in late spring.
A small amount of water is withdrawn in early spring from the upper 50
cm of old minesoils, perhaps by annual grasses. During the summer of 1976,
water is removed more uniformly from all depths to 150 cm. By late summer,
virtually all available water is removed from the root zone. As a conse-
quence of this depletion old minesoils were only recharged to 100 to 120 cm
in 1977. Below that depth the soil remained dry. The rapid water use at
depths is explained by the dominance of shrubs and half-shrubs on these sites.
Root biomass below 50 cm in old minesoils is greater than in natural soils
or new mine soils. Very little drainage probably occurs from old mine soils
because nearly all water is used by the plant community. The total amount of
water used in these soils was slightly greater than in other soils even
though they were often sandier and held less water. Site 3 which was leveled
in 1948 had higher water contents than most other soi18. A large amount of
coal was mixed into this profile which resulted in low bulk density. It is
possible that water-holding characteristics or the high hydrogen content of
the coal caused the unusually high readings. A similar water content curve
was found in the 1969-14 site which also contained abundant coal fragments.
The pattern of water use in new minesoils is somewhat similar to
natural soils except that water use begins earlier and is more rapid in the
spring. Water is removed from progressively deeper depths later in the
season. Water use rate slows considerably by mid-summer. During early
spring, from April 15 to May 31, 1977; 6.3 cm of water was removed from new
mlnesoils compared to only 4.4 em in natural soils and 2.9 cm in old mine
soils. This early water use is a reflection of the vigorous spring growth of
the introduced grasses common on this site. Water use declines in the summer
so that use during the entire growing season is slightly less than in natural
soils. New minesoils. have some plant-available water remaining in the root
zone of most plants even in late summer. As a result of the incomplete
water use, new minesoils were completely recharged in the spring of 1977.
Water is not used from below 100 cm on many of the youngest reclaimed soils.
This could be due to the lack of a well-developed root system, or the pres-
ence of soil layers which prohibit de~p root penetration. The older, well-
established plant communities on new minesoils have water use patterns which
are similar to natural soils (1972-13, and 1970-15). Water use on very
recent minesoils (1975-11) is minimal. It is possible that a large amount
of water drains from these soils which could affect the quality and quantity
of aquifers developing_in the spoils. Unvegetated sites generally have
higher run-off rates, however, which may prevent water from draining through
the soil.
100
-------
The total water stored in each soil when recharged was highly correlated
with the silt content (r = .73) and sand content (r = -.66) of the soils
(Wyatt, 1978). Water content was therefore highly influenced by soil tex-
ture. Water use at 50 and 100 cm from April 4 to June 15, 1977 was most
highly correlated with root biomass. Water use and root biomass were not
correlated at the 10 cm depth perhaps because other factors such as surface
evaporation also influence water movement in this zone (Table 12). Water use
was not well correlated with root biomass in old minesoils. This could have
occurred because most root weight at 50 cm and 100 cm in these soils consists
of large taproots which are not as effective in absorbing water. Water use
at these depths in the old minesoils occurred primarily after June 15 also.
Table 12.
Correlation (r) between root biomass (g/cm3) and water use (cm3/
cm3) from 4/4/77 to 6/15/77 at three depths in natural soils; old,
and new mine soils.
Soil Type Depth (cm)
10 50 100
Natural Soils .45 .98* .97*
Old Minesoils -.84 -.73 -.80
New Minesoils -.75 .99* .93*
*denotes a significant correlation at p < .95
Soil water is an important factor in the classification of soils (Soil
Survey Staff, 1975). Soil moisture regimes have been defined to account for
the influence of water on soil genesis and soil use. Based on information
collected in this study, soils in the Colstrip region are in an ustic soil
moisture regime but border on an aridic regime. These soils would not be dry
enough to be classified as Aridisols since they would have to be dry from
20-60 cm for more than one-half the time the soil temperature is above 5°C at
50 cm. For this to occur, the soils would need to be dry at 60 cm by late
June and remain dry until December. Soils in this study were not dry at this
depth until August and often were re-wetted in October or November. The
soils would qualify for aridic subgroups of Mollisols a~d Inceptisols.
Productivity of all sites was compared to water use and growing season
precipitation to evaluate the water use efficiency of vegetation (Table 13).
Perennial grass biomass, annual grass biomass, and total biomass were
correlated with growing season water use.and summer precipitation using
multiple linear regression techniques. The magnitude of the coefficient for
stored soil water and precipitation indicate the efficiency with which water
from that source was used. For example, a coefficient of 42.0 for stored
soil water in predicting total biomass means that for each cm of soil water
used, 42 kg/ha of vegetation was produced. It was found that stored soil
water was more efficient than summer precipitation in producing plant
material. This is a common finding as summer rainfall typically is lost by
interception and surface evaporation before it can be used by plants.
101
-------
Table 13. Vegetative production (kg/ha) in 1976 and 1977 was predicted from
the amount of stored soil water (cm) depleted from the upper 150
em, and summer precipitation (cm) using multiple linear regres-
sion. The magnitude of each coefficient for soil water and
precipitation indicates the efficiency with which that water was
used in producing biomass.
PREDICTED COEFFICIENTS R2
COMPONENT INTERCEPT Soil H?O PPT n
kg/ha
TOTAL BIOMASS
ALL SITES 696 42.0 9.6 .27 20
NATIVE 152 51.4 16.4 .24 4
OLD SPOIL 536 81. 7 -15.8 .64 5
NEW SPOIL 1409 16.0 -31. 0 .24 6
PERENNIAL GRASSES
ALL SITES 140 27.2 13.0 .19 20
NATIVE -453 50.7 35.2 .82 4
OLD SPOIL -613 19.5 91.6 .19 5
NEW SPOIL 1437 4.8 -55.0 .73 6
ANNUAL GRASSES
ALL SITES 271 2.9 -16.0 .13 20
NATIVE -533 44.0 5.9 .47 4
OLD SPOIL 203 14.8 -23.1 .31 5
NEW SPOIL 217 7.2 -22.0 .25 6
Water was used most efficiently by old minesoils in producing total
biomass which consisted mostly of half-shrubs and annual grasses. However,
more perennial grass biomass was produced per unit of water used on natural
soils. Total biomass and perennial grass production on new minesoils did
not vary much with differences in water use and precipitation in 1976 and
1977. Since many new mines oils are not fully depleted of water during the
growing season, water availability may not be the most critical factor in
determining productivity. Plant communities on natural soils used summer
precipitation more efficiently than either old or new minesoils. Summer
precipitation did not, in fact, increase minesoil productivity at all. This
difference in use of summer precipitation can be explained by the composition
of the plant communities on each site. Both warm- and cool-season grasses
and forbs are common on native soils. Some plants are active during all parts
of the growing season to utilize water. By contrast, very few warm-season
species existed on the new mine soils. Most plants had therefore senesced by
the time the summer rain fell. Th~ only active plants on old minesoils during
most of the summer were deep-rooted half-shrubs and shrubs. These- plants
obtained their water primarily below 50 cm during this period and thus could
not use summer precipitation which remained in the uppermost soil layers.
102
-------
Soil Water Potential
Water potential readings obtained with the thermocouple psychrometers
(TCP) did not correlate with the changes in water content observed with the
neutron probe, and thus were considered inaccurate. Soil water potential
data ~i11 not be formally discussed in this report. Considerable care must
be. taken when installing and reading TCP's to avoid temperature gradients in
either the TCP or the microvo1tmeter used for reading.
The desorption characteristicsoi'each soil were measured by analyzing
cores from the neutron access holes, and undisturbed soil clods from a backhoe
pit. Soil water content of these samples was measured after equilibrating at
0, 0.1, 0.3, and 15 bars. These data were used to indicate zones of water
availability on the soil water content figures (Figures 39 to 53). Water
retention at 0.3 and 15 bars were positively correlated with silt content and
inversely correlated with sand content. Natural soils held slightly greater
water content than minesoi1s at these potentials because of their lower sand
and higher silt and clay content. The water-holding capacity of natural soils
were slightly higher than minesoils .
Soil Temperature
Soil temperature at 15, 50, 90 and 150 cm was measured monthly from
June, 1976 to August, 1977 (Table B-4). Sensor units were removed from the
field for calibration and cleaning during the winter of 1976-1977.
Mean annual soil temperature (MAST) at 50 cm is used in the definition
of soil temperature regimes in the soil taxonomy (Soil Survey Staff, 1975).
To calculate the MAST, temperature on July 1, October 1, January 1, and April
1 were graphically inferred from a plot of soil temperature data. The aver-
age of these dates gives the MAST. All soils in this study had mesic soil
temperature regimes or MAST greater than BOC. Some of the soils on north
aspects which remained wetter through much of the year were borderline on a
frigid temperature regime (MAST < BOC).
Old minesoi1s had somewhat higher soil temperatures than native soils
while new m!nesoi1s had lower temperatures (Table 14). Old mines oils are
drier than other soils because plants use water most fully on these sites.
Since water has a large heat capacity, a drier soil would be expected to
become warmer than a wet soil. A large litter layer which was observed on
new minesoi1s could account for the lower soil temperature on these soils.
Soil temperature at 50 cm in new mine soils showed less seasonal fluctuation
than in other soils. This could also be accounted for by the litter layer.
103
-------
Table 14. Soil temperatures at 50 cm in spring, summer, fall, and winter
were graphically inferred from a plot of all soil temperature
data. Mean annual soil temperature was calculated from the
mean of seasonal temperatures.
Date Largest
7/1/7 5 10/1/76 1/1/77 4/1/77 Mean Ann. change in
Site Soi1,Ternperature(C.) Soil (C.) Temp. (C.) Temp.
Natural Chinook-1 18 13 -2 6 8.75 20
soils Boxwell-2 16 15 0 6 9.25 16
Chinook-8 19 17 0 7 10.75 19
All 9:6 T8.3
Old mine 1928-7 19 14 0 6 9.75 19
soils 1928-9 18 16 0 7 10.25 18
1929-10 18 15 -.5 7 9.9 18.5
All ro:o 18.5
New mine 1975-11 16 14 0 7 9.25 16
soils 1973-12 16 10.5 .5 8 8.75 15.5
1972-13 14 12 2 5 8.75 12
1970-15 15 14 2 7 9.5 13
All B:9 14.1
104
f''''
-------
SECTION 9
ROOT CHARACTERISTICS
A field root counting method which can be used to obtain root biomass
was used to characterize roots in the field (Schafer and Nielsen, 1978).
Natural soils, old minesoi1s., and new minesoi1s differed in total root
biomass, root distribution with depths and the size of roots.
Root Biomass
Old minesoi1s had nearly twice as many roots as natural soils (Table
15). Biomass in the upper 100 cm averaged 743 g/m2 which was slightly less
than in Colorado grasslands (Bartea and Sims, 1974). New minesoils had less
roots than natural soils. It appears that either several years are required
for mature grassland root systems to develop, or that introduced grasses do
not produce as much root biomass as native vegetation.
Table 15. Root biomass, the proportion of roots in surface horizons, and the
fraction of roots in various size classes is shown for natural
soils and minesoils. Values are the mean of 5 sites.
Biomass Root Size (min)
2 Percent in .1-.5 .5-1 1-2 2-5 >5
Soil glm Upper 25cm %
Natural 404 71 32 44 4 20 0
Old 743 63 18 22 22 29 10
New 318 83 34 33 19 7 7
Roots in the upper 25 cm made up 71% of the biomass in native soils and
83% in new minesoi1s., which were dominated by perennial grasses. Many of
the youngest minesoi1s had over 90% of their roots above 25 cm which
suggests that shallow roots develop first in reclaimed plant communities. By
contrast only 63% of the roots in old minesoils occurred above 25 cm. This
is a reflection of the half-shrub and shrub-dominated plant community. The
abundance of deep roots in old minesoils explains the more complete use of
water below 50 cm.
The size of roots in natural soils and new minesoils was similar. More
than 75% of the root biomass consisted of fine and very fine roots « 1 nun
diameter). Fine (1-2 mm)or medium-sized roots (2-5 mm) made up the remainder
of the root weight. Old minesoils had more medium and coarse roots (>2 mm)
as a result of the abundance of taproots from A~temesia d~acuncuZus and other
105
-------
shrubs. Only 40% by weight of the roots in old minesoils were very fine and
fine. Since large roots are less effective iITwater uptake and have less
length per unit weight, roots in old minesoils were probably less efficient
per unit weight in taking up water than the more fibrous roots of perennial
grasses. More root weight is maintained in deep-rooted plant communities,
but water uptake per unit weight of roots is less than in communities with
shallow fibrous roots. Deep-rooting provides the advantage of a larger soil
water reservoir but exists at the expense of aboveground production since a
larger fraction of the photosynthate must be used in the growth and mainten-
ance of the root system.
32
P Uptake
Radioactive phosphorus was injected at various soil depths. Vegetation
growing above each injection site was monitored for uptake of phosphorus. If
p32 was found in the plant top, it was assumed that roots were growing at
that injection depth. Shielding of the injection device prevented comtamin-
ation of sides of the hole when p32 was placed in the soil. The absolute
amount of p32 taken up by the plant top was used as an index of root activi-
ty. Corrections were made for p32 decay and residual p32 from earlier
measurement dates using an equation derived in Appendix C. The absolute
amount of p32 uptake was ~robably influenced not only by root activity but
also by phosphorus availability. and solute transport mechanisms within the
plant.
32
Radioautographs from two plants which had taken up P were obtained
(Fig. 54). The radioactivity was most concentrated in the young, actively
growing portions of the plants which in Artemisia frigida is at the meriste-
matic tip of young stems, and is near the ground level in Stipa aomata.
Some p32 was also found in older stems and leaves, but was less concentrated.
Comparison of radioactivity in grasses, forbs, and shrubs is complicated by
this differential pattern of phosphorus accumulation. All readings were
taken on the most radioactive portion of each plant.
Some natural background levels of beta radiation exist in the environ-
ment. Several plants outside the study area were surveyed for radioactivity.
No significant differences in background radioactivity were found in
different species or at different sites. A single value of 13 counts per
minute (cpm) was used as the background radioactivity level. Only radio-
activity above 13 cpm would indicate p32 uptake. Most radioactive plants had
readings of 100 to 10,000 cmp.
Field radioactivity readings were discussed by Wyatt (1978) and appear
in Appendix C. Relative p32 uptake between dates of measurement was
calculated, and is termed the plant activity index (PAl) because it is a
function of root activity, and plant transport of solutes. A summary of
plant activity index values by soil depth and plant type is found in Table
16 and Table 17.
One objective of this study was to find the maximum rooting depth of
common range plants in the Colstrip area both on undisturbed soils as well as
minesoils (Wyatt and others, 1978). Knowledge of the required depth of the
106
-------
Fig. 54. Radioautographs of a grass (needle-and-thread)
and a half-shrub (broom snakeweed) showing p32
accumulation in the meristematic regions.
Table 16. Summary of plant activity index (PAl) values for various /
vegetation types on Colstrip so ils during 1975 and 1977.
80th
SOIL TYPE VEr.ETATION TYPE 6/27 7/16 8/19 t'n6 ~/ 17 'II 'ill] l'>/lS '/9 7/19 7/31 1977 Yt'arl!
NATURAL PERENNIAL GR. 5511'" 12711 -6911 JaD 94' ,,' 8210 4724 }3,,28 ]0128 131)17 144122 121155
SOILS ANNUAL GR. JS' 1223 -251 '08 '08
7)9 11'.510 14)) " 13) , llOS ~28 8 214 B -240'1 4 (~ t.. 1 696)
FORBS 12C~ f:,.. 14
,,' ,,' 41' 4513 '0' 'if.] 253 '0' ' ,,' 11))2 3822 41)')
SHRUBS -24
5728 12629 -1019 67 'TI) If,12 5)15 4018 1.,4]6 ')640 25540 2'. 108185 96261
ALL 55
OLD PI:RENUIAL GR. 8) ,5 ,) 6" ,5 " 4)11 10513 -1)019 -11614 -24" -28"8 -2479
MINE ANNUAL GR.
SOILS 105 2)10 Q' 1621 ,,, 206) 251 ' -2DJlo -712 -3817 -8)1:\
FORES lor -1)6
SHRUBS ))7 5)11 .8 )426 ,1 142 1962 152 -31) -129 -662 ,21 2147
ALL 2015 ))26 8" n58 ,7 )0' 9]16 89" 13021 -9527 -468 -Z)lOh -1146
," 5'8 1041 5)5 15:;11 13 ,19 0'9 -12620 7187 11128
NEW PERENNIAL GR. 21n 108
HINE ANNUAL GR. )2 13' _1)1 -).:. ,1 -1061 -S22 -196
SOILS ,,6 1087 ,,' 7219 11' 100) -S8) 12) -42) -80) -1117 ))36
FORBS
SHRUpc 65 -,) ,8 " " .' _1)1 ), ,"
ALL 1919 4225 1)28 2S72 '1' 14)14 7)17 ,24 -425 -11525 6112 14184
ALL PERENN IAL GR. 2825 6028 -21 J2 2085 5617 812(; 79)4 4756 2861 6962 10621 60277 51 )62
SOILS ANNUAL GR. 2,6 95' -282 )912 2' -1061 -522 2614
FORBS 4920 qa27 5415 ]262 126 1409 9011 2012 )715 5815 -1927 2075 441)7
3811 4021 1515 )247 48) )95 79' )98 . -414 , 1849 2596
SHRUBS -19" 19
ALL 3652 6980 56' 39196 4526 8)43 8151 4276 1186 5492 )032 47403 44599
. the number of reading!! obtained to compute the !!lean
Superscript repre!!ents
107
-------
Table 17.
Summary of plant activity index (PAl) values representing
p32 uptake from various soil depths of Colstrip soils
during 1976 and 1977.
NEW HINE
SOILS
Depth loth
(em) 6/27 7/16 8/19 1976 4/17 5/1 5/13 6/15 719 7/19 7/31 1977 Years
15 925 1797 -797 6419 689 59'0 '25'0 56'9 7819 17219 6811 9391 91116
46 646 1697 744 11017 l' 273 256 489 26" 42411 -2197 8548 10465
76 669 '23'0 ,5 7425 1092 572 2)2 155 2046 3506 1233 16026 11851
107 192 -42 ~4 122 4162 16192 8692 129& 48912
137 72~ -32 192 167 " -2' -12 -1042 -,, -307 -114
183 103 4' q4 94
15 355 436 -143 28'4 ~4 397 12211 50" -78'2 -13512 -614 -1061 -375
46 195 574 202 ))11 .3 04 275 18,5 -2576 -2567 -40J -6238 -4049
16 93 347 ,5 2115 73 753 2743 -6' 10810 5625
107 ,2 264 -13 129 129
137 ,4 274 168 168
15 496 396 248 3520 476 17713 77'6 1'8 -13'8 -'41'8 1189 '9'09
46 ,5 1001 11 4019 254 215 -585 -614 2033
76 ,5 166 105 ,16 l' -2' -,, 26' -11' -40' -46 422
101 " ,3 153 .1 " 38' -'5' -83 8'0
131 ,2 113 -45 ,'0 2' 2' ,ll
15 58'6 9219 -2281 4353 4819 10530 10331 3548 ~49 -1849 34'5 38241 39300
46 )216 111'8 2613 6347 ,4 121 26" 8,'8 -5222 11223 -'65'0 '6'00 31147
16 )111 6823 ,15 2555 143 313 153 149 '44'0 428'0 914 12442 6891
107 105 119 16 1020 83 2903 10743 8692 5)211 19531
131 115 ,9 1111 1025 " -2' -12 -693 -11 -268 ,33
183 103 4' " 44
NATURAL
SOILS
OLD HINE
SOlLS
ALL
SOILS
*8uper8crtpt represents the nuaber of read1nss obtained to compute the mean.
root zone is important in mine reclamation so that potentially phytotoxic
overburden materials, saline materials, and physical barriers to root growth
can be eliminated from that depth. The maximum observed rooting depth of 41
species which took up phosphorus is shown in Table 18. These data are basad
on a limited number of injections of small spatial extent. The values
reported do not necessarily represent the maximum rooting depth except for
the most common species. These are minimum estimates. Plant roots of many
perennial grasses. forbs, and shrubs extend to at least 137 cm on natural
soils, old mines oils , and new mines oils . Stipa aomata had roots at least
as deep as 183 em on native soils. Plants on all sites can probably obtain
water or nutrients from the upper 150 to 200 cm of soil at all sites.
32
An analysis of variance was conducted on P uptake data from 1976
(Table 19). Significant differences in uptake occurred between groups, dates
of measurements, and depth of uptake. In addition, the group by date inter-
action and group by depth interaction were also significant which indicates
that the pattern of change of p32 uptake on successive dates and with
increasing depth was different for natural soils and minesoils. These
patterns will be discussed in detail in ,the following sections. The date by
depth interaction was also significant.
The average plant activity index on each measurement date for each soil
is shown in Table 20. These are the average of all species at all depths
which took up phosphorus. The average PAl 1s greatest for native soils in both
1976 and 1977, and on 6 out of the 10 measurement dates during the study.
The smaller PAl in minesoils could be caused by 1) less root biomass,
108
-------
Table 18. Maximum observed rooting depths using p32 tracer in Co1strip
soils.
Rooting Depth (em)
Species Native Soil Old Spoil New Spoil
Grass
Agropyron aristatum 76
Agropyron dasystaahyum 46
Agropyron eZorzgatum 137
Agropyron smithii 46 107 15
Agropyron spiaatum 76
Agropyron traahyaauZum 107 137
Agropyron triaophorum 46
Avena fatua 46
BouteZoua graaiZis 76
Bromus inermis 76
Bromus teatorum 76
CaZamoviZfa ZorzgifoZia 46
KoeZeria aristatum 76 76
Poa pratensis 46
Poa sandbergii 46
S tipa aomata 183 137
Forb
Agroseris gZauaa 107
Ambrosia psiZostaahya 76 137
AstragaZus aiaer 15
CaZoahortus nuttaZZii 15
Gaura aoaainea 137
GrindeZia squamosa 15
Laatuaa pu Zahoha 107
Laatuaa serrioZa 46
Leuaorarinum montanum 46
MeZiZotus offiainaZis 137 137 15
Mediaago sativa 76
PetaZostemon purpureum 76 15
PsoraZea esauZenta 76 76
SaZsoZa kaZi 46
Tragopogon dub ius 137 46
Shrub
Ankanaria species 15
Artemisia aana 15
Artemisia draaunauZus 137 137
Artemisia frigida 46 15
Artemisia Zudoviaiana 76
Chrysopsis viZZosa 46 46
Chrysothamnus nauseosus 15
Chrysothanmus visaidifZorus 107
Gutierriza sarothrae 64
Rosa species 15
109
-------
Table 19. Analysis of variance fo p32 uptake (counts/minute) showing
sources of variation for the 1976 growing season.
SOURCE DF SS MS F P
GROUP 2 2336349 1168174 15.47 < .001
DATE 3 1193790 596895 7.90 .003
DEPTH 5 4554351 910870 12.06 < .001
GRP X DATE 4 840044 210011 2.78 .055
GRP X DEPTH 10 2926526 292652 3.88 .OQS
DATE X DEPTH 10 1981030' 198103 2.62 .032
ERROR 20 1510317 75516
TOTAL 53 15343410 289479
Table 20. Average plant activity index (PAl) values from all species
and all soil depths is shown for the 1976 and 1976 growing
seasons on Colstrip soils.
1976 1977 AveraRe
Soil type 6/27 7/16 8/19 4/17 5/1 5/13 6/15 7/9 7/19 7/31 1976 1977 Both
Native Soils 57 126 -10 70 53 40 44 96 255 55 67 108 96
Old Mine Soils 20 33 8 30 93 89 -130 -95 -46 22 -23 -7
New Mine Soils 19 42 13 41 143 73 -4 -115 25 6 14
2) less affinity for phosphorus, 3) phenological differences in plants within
each community, or 4) less availability of added p32. Old minesolls have
nearly twice as much root biomass as natural soils, and identical species
growing on natural soils and minesoils reflect the same relative differences
in PAl. Differences in PAl are probably therefore due to differences in
phenology and p32 availability. Plant communities on new mines oils cease to
take up p32 by mid-June in 1977. Water use was also observed to decrease
during this period, probably because of initiation of summer-dormancy in the
introduced perennial grasses dominant on new minesoils. The activity of
surface roots ceased b~ late June in old minesoils even though deep roots
continued to take up P 2. Roots at all depths in natural soils continued to
take up p32 through July. These phenological patterns account in part for
differences in the PAl. Minesoils have a slightly higher pH than natural
soils and contain up to 10% CaC03 while most natural soils are free of CaC03
in the upper 50 cm. Phosphorus can precipitate on CaC03 surfaces and is
rendered unavailable to plants in the process. In addition, phosphorus
availability to plants tends to decrease with increases in-pH between 7.5 and
8.5. Soil factors which influence, phosphorus availability probably also
affect the PAl values in these soils.
Comparisons of PAl between 1976 and 1977 must be made with care since
injections were made at different times of the year. Qualitative comparisons
are valid, however. The main difference between the two years is in the
depth of p32 uptake (Table 18). Uptake occurred from deeper depths in larger
amounts in 1976 than 1977. This occurrence can be explained by precipitation
patterns. A wet spring in 1976 caused soil water to be recharged throughout
the root zone while a dry summer required plants to obtain water from deep in
110
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the soil. Soils were not as fully recharged during the dry spring of 1977,
and higher than normal precipitation during the summer provided much addi-
tional water near the soil surface. Plant communities apparently have the
capacity to respond to climatic fluctuations by increasing root activity
where water is most available. As a result, marked differences in root
growth probably occur from year to year.
Increases in the PAl of plants should indicate increases in root
activity. A value of zero indicates no uptake of p32 and thus no root
activity. Many negative values of PAl were found, however. Plant activity
index below zero does not agree with the simplified interpretation of PAl
values originally assumed. Other factors must influence PAl. Sosebee and
Wiebe (1973) studied the movement of foliar-applied p32 in crested wheatgrass
(Agropyron aristatumJ. They found that as plants approached summer dormancy
in August, p32in leaves, internodes, and the inflorescence decreased to near
zero. At the same time, the radioactivity of the crown and plant roots
increased to a maximum level. The same flux of materials into the root sys-
tem late in the growing season was indicated by Ares and Singh (1974) in
their model of the dynamics of a shortgrass root system. Therefore, PAl
reflects the balance of upward movement of p32 from active roots, and down-
ward movement of previously assimilated p32 into roots and crowns for stor-
age. When downward transport exceeds uptake, negative values for PAl are
obtained, which indicates that plant senescence is approaching.
Perennial grasses on natural soils remain active throughout the April to
August growing season in 1977 (Fig. 55). Peak PAl values occurred in mid-
July which was two weeks after several cm of rain fell in the area. Perenni-
al grasses on old and new spoils had peak PAl values earlier in the growing
season while senescence occurred as early as late June or early July. The
maximum plant activity index on new minesoils occurred in early May when
introduced grasses on the spoils were greening up. Forbs show the same PAl
pattern as perennial grasses except that senescence occurred about two weeks
earliers on all sites. Shrub root activity was less than either grasses or
forbs probably because the taproot system has fewer numbers of roots in a
volume of soil than do fibrous-rooted grasses.
The depth of active roots in natural soils; old and new minesoils is
shown in Fig. 56. Old and new minesoils follow a similar pattern. Root
activity at 15 cm begins early but ceases by late June when water has been
depleted and senescence is approaching. Peak root activity at 15 cm in new
m1nesoils, old minesoils, and natural soils occurred in late April, mid-
May, and mid-July respectively. As a consequence of senescence of plants on
mtnesoils, the abundant summer precipitation during 1977 could not be used
for additional growth. A similar pattern of root growth occurs at 45 cm
except that plant ac~ivity peaks later in the season. Plants on old mine
601ls take up more P 2 than plants on new minesoils at this and deeper
depths probably due to higher root biomass. Minesoils rely almost entirely
on root activity below 50 cm during June and part of July when the plants are
approaching maturity. Although uptake of p32 at 15 cm continues in natural
soils through July, an increasing proportion of the total uptake comes from
deep soil depths. Although roots below50cm comprise less than 10% of the
total root biomass, these deep roots are critical in supplying water and
111
-------
200
100
-100
o
PER. GRASSES
A
200 FORBS
X 100
W
0
Z 0 A
>-
~ -100
>
~
U
-------
200 15em
100
0 A
-100
200 45em
X 100
W
0
Z 0
>-
...... -100
>
......
U
<:( 200 76 em
...... 100
Z
<:(
..J
a.. 0
-100
200
100
Fig. 56.
A
A
107em
~619
"\ NATIVE
~ bS69
~416
o
A
DATE (1977)
Average plant activity index for
uptake from several soil depths
through the 1977 growing season.
113
-------
nutrients to plants late in the growing season.
To better understand the processes in soil that influence root growth
and plant senescence, and how individual species respond to environmental
changes; plant activity index of several species was compared to soil temper-
ature and soil water content in an undisturbed soil (Fig. 57). It appears
that root growth initiates at deeper depths as the growing season progresses.
The date of initiation corresponds closely to the movement of the 11 to 14°C
isotherm as the soil warms. Uptake of p32 by root growth becomes less than
downward transport when PAl falls below zero. This decrease in PAl occurs
when the soil dries to near the permanent wilting point. Since the soil at
deeper depths did not dry to 15 bars during the observation period, PAl
remained positive. Stipa aomata which has a dense, fibrous root system,
exhibits the highest PAl values perhaps because it has more roots in contact
with the injected p32. The initiation of growth of Stipa aomata~ KoeZeria
aristata~ Tragopogon dubius~ and Artemesia frigida was nearly the same at
each soil depth. BouteZoua graaiZis~ a warm-season grass, appeared to begin
growth slightly later than other species.
Soil temperature appears to control the initiation of growth in these
soils. New minesoils have slightly lower soil temperatures and warm more
slowly in the spring than other soils, perhaps due to large litter accumula-
tions and wetter soils. It takes nearly two weeks longer for new minesoils
to reach 11 to 14 CO at any depth than other soils because these soils are'
wetter and have thick litter layers. Limited water availability influences
the length of time roots can remain functional. When the water potential
nears 15 bars, most root activity ceases. Sandy soils with less water-
holding capacity such as the old mines oils dry out sooner than other soils.
As a result, droughty soils have a shorter effective growing season. Genetic
differences between plant species cause plants to respond differently to
changes in the soil environment. Plants adapted to dry climates or short
growing seasons will begin growth earlier or sustain it later than poorly
adapted plants under similar soil temperature and water availability. Plant
ecotypes adapted or bred for the soils and climate of a particular region
should be most successful in establishment of self-sustaining reclaimed plant
communities.
114
-------
~
~ I~gg 15em ~
t;~ 10
eto 0
I-Z
z- -10
:3 -100
~ -1000
a::
11.1 40 SOIL
!c( 30 WATE
~~ 20
~- 10
(/) 0
- .
. -
. -
- -
- -
- .
!
-------
SECTION 10
MICROBIOLOGICAL ACTIVITY
Adenosine triphosphate (ATP) is an essential part of all living cells.
The ATP content of microorganisms remains constant throughout all life stages
and ATP quickly disintegrates after the death of a cell. Measurement of ATP
activity in soils is, therefore, an excellent index of microbiological
activity in the soil. Maximum ATP concentration in samples collected during
August, 1976 varied from 107 to 109 fglg in the 15 soils studied (Figs. 58-
60). The relative distribution of ATP with depth was similar in all soils.
Maximum ATP content occurred in the top 1 cm in most cases. Adenosine
triphosphate concentration decreased rapidly with depth until equilibrium
levels of lxl07 to 5xl07 fglg were reached at about 50 cm in natural soils
and 30 cm inminesoils. Differences were not apparent between maximum ATP
activity in natural soils and minesoils. Natural soils generally had higher
ATP activity than minesoils from 10 to 50 cm, however. It appeared from the
pattern of ATP distribution with depth that microbiological activity was not
strongly influenced by differences in water content. When samples were taken
in August, 1976, a dry summer, soils were dry throughout most of the root
zone, but were moist below 100 to 150 cm. Microbiological activity was
probably more influenced by the availability of food (organic carbon) and
nutrients than by water. Organic carbon content of all soils was highest
near the surface and decreased with depth which paralleled the distribution
of ATP. Natural soils had more organic carbon than minesoils from 10-50 cm
which may explain the differences in ATP activity at these depth. It is
interesting to note that relative differences in ATP activity between mine
soils and natural soils were not as large as differences in organic carbon
content. Although less organic carbon occurred in minesoils , ATP activity
was nearly the same which suggests that the organic matter in minesoils is
less decomposed (and thus yields more energy) than organic matter in natural
soils.
The distribution of ATP in the 1975-11 site, the youngest minesoil,
differed from ~he pattern described above. Maximum ATP concentration was
only about 5xlO! fglg and occurred at 20cm rather than near the soil surface.
This difference' in ATP distribution is ;probably a result of the youth of this
site. A comparison of the 1973-12, 1972-13, and 1970-15 sites indicates that
ATP distribution in minesoils becomes more similar to the pattern found in
natural soils with increasing age.
The 1948-3 site and the 1969-14 site each had very low maximum ATP
levels. These two soils are unique in the study in that each contained a
large volume of coal fragments. The 1948-3 site in particular had fine coal
particles distributed throughout'the sQ!l ~trix. It is possible that coal
inhibits microorganism populations in some way.
116
-------
o
o
25
50
75
E 50
,g
I
I-
a..
W
0100
Fig. 58.
150
/
CHINOOK - I
] 50
-
I
I-
a..
W
0100
o
o
150
NATURAL SOilS
ATP (fg/g sail} x 107
100 0 25 50 75 100
BOXWELL - 2
25
ATP (fg/g soil) x 107
50 75 100 0 25 50
o
25
RIEDEL - 6
239
ETHRIDGE - 4
75
CHINOOK - 8
ATP activity in natural soils, August, 1976.
117
50
75
100
284
100
-------
E 50
,g
I
I-
0-
W
0100
o
o
150
25
50
75
OLD MINE SOILS
A TP (fg/g soil) II 107
100 0 25 50 75 100
o
Fig. 59. ATP activity in old minesoils, August, 1976.
1928-5
] 50
-
I
I-
0-
W
0100
150
225
1928-7
o
o
ATP (fg/g soil). 107
50 75 100 0 25 50
25
170
1929 - 10
1948-3
118
25
1928 - 9
75
50
75
100
100
-------
E 50
S
:r:
r-
CL
w
0100
o
o
150
25
50
150
75
NEW MINE SOILS
A TP (fg/g soil) x 107
100 0 25 50 75 100
o
1969 - 14
] 50
-
:r:
r-
CL
W
0100
322
128
1970- 15
o
o
ATP (fg/g soil) x 107
50 75 100 0 25 50
25
1973 -12
1975-11
Fig. 60. ATP activity in new minesoils, August, 1976.
119
25
1972 -13
75
50
75
100
100
-------
Selected soils were analyzed for ATP content again in June, 1977 (Fig.
61). Samples were collected every 10 cm to 30 cm in depth so that caution is
needed in making direct comparisons between June, 1977 and August, 1976 ATP
activities. No apparent differences existed between ATP concentration in
natural soils and minesoils. It is interesting, however, that three of the
five soils studied had maximum ATP levels at 30 cm rather than near the soil
surface. In addition, ATP activity at 20 and 30 cm was higher in these
samples than in August, 1976. Higher ATP levels could have been caused by
increased nutrient or food availability. This agrees with the findings of
Bartos and Jameson (1974) who found that root decomposition rate reached a
maximum in early summer in Colorado grasslands. Haigh a976) recorded the
highest yearly soil nitrate levels during June in several Montana soils.
Large differences in ATP activity were found for the three mines oils
deposited in 1928 (1928-5, 1928-7, and 1928-9). These soils are edaphically
very similar. These relative differences in ATP activity were often reversed
on other sampling dates which suggests that ATP activity is an extremely
variable property.
Adenosine triphosphate activity was measured again in October, 1977 on
five selected soils. No differences between natural soils, old and new mine
soils were apparent (Fig. 62). Maximum ATP concentration again occurred near
the soil surface as in the August, 1976 samples. The average ATP activity in
the upper 30 cm of these soils was the highest measured in the study. It is
possible that increased nutrient availability, or increased water content
accounted for the higher ATP levels. Weaver and Forcella (1978) found that
maximum annual levels of available phosphorus, ammonium, and potassium
occurred in September or October under six vegetation types in western
Montana.
Conditions may be most favorable for microbiological activity both early
and late in the growing season when nutrients, soil water, and food sources
(dead roots) are at a maximum. During the winter, soil temperature is too
low for maximum growth while during the midsummer, grasses, forbs, and shrubs
may compete effectively for limited water and nutrients.
Rhizosphere, rhizoplane, and free-soil ATP activity values are shown for
14 plant species in Table 21. The rhizoplane is the root surface, the
rhizosphere is the soil zone surrounding the root, while free soil is
material not in close contact with plant roots. Microbiological activity was
highest in the rhizoplane for all 14 plant species analyzed. Rhizoplane ATP
levels ranged from 9xl08 to 2l5xl08 fg/g. Rhizosphere ATP activity was
slightly higher than free soil activity for 8 of 14 plants. Even though
rhizoplane ATP activity was higher than either rhizosphere or free soil
levels, ATP in the rhizoplane comprised only a small portion of the total ATP
in each sample. This occurred because only about 1% of each sample was in
the rhizoplane zone.
Free soil, and rhizophere ATP activity were exceptionally low in the
1948-3 site. For these samples, the majority of the ATP in the sample was
found in the rhizoplane even though only 0.5 to 3.2% of the sample was
rhizoplane material. As suggested in an earlier section, it 1s possible that
120
-------
E
s 10
I
I-
a..
w
o 20
30
Fig. 61.
o
o
25
50
RIEDEL - 6
e
o 10
-
I
I-
a..
w
o 20
30
75
ATP
100 0
(fg/g soil) x 107
25 50 75 100
1928- 5
o
o
ATP (fg/g soil) X 107
50 75 100 0 25 50
121
146
25
1928 - 9
1948-3
ATP activity in selected soils, June, 1977.
o
25
1928 - 7
75
50
75
100
100
-------
g 10
-
I
I-
Cl.
W
o 20
30
o
o
25
50
75
ATP
100 0
(fg/g soil) X 107
25 50 75 100 0
CHINOOK - 8
o
o
25
AT P (fg/g soil) X 107
50 75 100 0 25 50
154
25
1972 -13
Fig. 62. ATP activity in selected soils, October, 1977.
RIEDEL - 6
]' 10
-
I
I-
Cl.
W
o 20
30
1948 - 3
122
1928 -7
75
50
75
100
100
-------
Table 21. ATP in free soil, rhizopshere and rhizoplane
Site Free Soil Rhizosphere Soil Rhizoplane
8 8 8
fgATP!gxlO % of Total fgATP!gxlO % of Total fgATP!gx10 % of Total
Riedel-6 Bromus teatorwn 5.08 84.0 5.65 15.0 24.9 0.4
Riede1-6 B. teatorwn 6.75 90.0 7.63 2.5 215.0 7.4
Riede1-6 /U'temesia
frigida 4.97 79.4 6.79 13.6 12.1 6.7
Chinook-8 Stipa aomata 7.85 85.8 7.72 2.3 62.3 11.8
Chinook-8 Ch:r>ysopsis
vi Uosa 4.29 84.1 11 . 50 6.3 80.0 9.5
Chinook-8 /U'temeisa
...... frigida 7.53 91.6 10.10 2.6 72.2 5.8
N
w 1928-7 Agropyron
smithii 3.13 91.4 1.84 4.0 9.07 4.4
1948-3 Solidago
missouriensis 2.93 57.9 1.28 2.6 55.8 39.5
1948-3 Taraxaawn
offiainale 0.21 46.4 0.43 1.2 48.7 52.4
1929-10 Solidago
missouriensis 3.34 81.5 8.48 4.5 55.9 14.0
1929-10 Agropyron spiaatwn 10.20 87.8 19.30 4.0 52.0 8.1
1972-13 Agropyron
aristatwn 15.20 87.3 10.60 7.2 74.0 5.6
1972-13 Bromus inermis 4.95 91.2 1.63 0.9 38.0 7.9
1972-13 Me Zilotus
offiaianalus 12.40 91.8 1.52 0.6 62.4 0.1
-------
the abundant coal in the 1948-3 site inhibited microorganism populations
except on the surfaces of plant roots.
124
-------
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132
-------
Schafer, W.M., G.A. Nielsen, and D.J. Dollhopf. 1977. Soil genesis hydro-
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133
-------
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Common-
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Geoderma 15:1-19.
1976.
The fate of P during pedogenesis.
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(in press).
134
-------
Weaver, J.E.
286.
1919.
The ecological relations of roots.
Carnegie Inst. Publ.
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Carnegie
., and R.W. Darland. 1949. Soil root relaticnships of certain
native grasses in various soil types. Ecological monographs. 19:
no. 1:305-338.
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under six Rocky Mountain vegetation types. (in press).
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maturity sequence of New Zealand basaltic soil profiles. Soil Sci.
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change and soil moisture loss under frozen conditions. Soil Sci.
98:244-248.
Wyatt, J.W. 1978. Soil water and root characteristics of 1- to 53-year old
stripmine spoils in southeastern Mont. Unpubl. MS thesis, MSU, Bozeman,
MT.
., D.J. Dollhopf, and W.M. Schafer. 1978. Root distribution in
1- to 48-year old stripmine spoilsin southeastern Montana (in press).
Yaalon, D.H. 1975. Conceptual models in pedogenesis:
functions be solved: Geoderma 14:180-205.
Can soil-forming
135
-------
Table A-I.
~I IL ~,..'
'l' ~,' '~. r I, '-I.:
lrrfTI'-':
(I ,v. P If :,"":
~ IT I '"".: 1 t I
)HP': .
'1' ".'I'-t,IQI
) r It 1 t ..., ~ . 11. ~ ,
100" .Hll:
,( f( IPI":' I . .
,,( ~ -, . P Il 11 . :
,~, 'II t..- ',' ~ , :
. I( ~ [ ~ t l I ' , :
V",111I1'.
"" ~ "..! .. 1 .
,,(111/'"
APPENDIX A
80il Characterization
Pedon Description of Chinook-l soil.
(JI'Io(L,'
-lr;r.
P,'1 11) I
'01 ",, hi 1'''', \In ,I, 1,101. '''U. I.!I IIflF) ~III 0' COlS"', "'.
,t'll l.llt~; Cr.H S' -1('" t '1"0
..,,,,,,,:
r.l"',,:
.'.."..JI:
",,','1t:
"1'1":
'UVUIO"': u'fu, IIttlll! 1II01n" 5""LfOI IU'US1
n..n: Cf;..(nf 1"'(11 ..a.,"
$UII'U: ,,~ '1HlftS' 111111"': .l4 DECi'HS f
su'''{': OturU , IIIINU': OltllU f
"nH: fl,c'nT II ,,,,n: H "'1£1 UtLf
(:""HIJl '1(110.. If''JT~ -- UP'f': C'IS 'III LO""~ He ell
L.,U.'(J (ll~~: 'lull C"It-ED
. 'I 'il ~ ~ 11 l' ), f;" II. I
II. . "I ( . ~ t " I
.'It t.~ f I" r
co.
~ "'.
"'\i,"'1 I' .frlf'
. \ 1 'I' . 11' I r u" r ~" .... t r, t
,..,. .,! ~, ,,, r 01 p' I ~:. I r "
r. ~.,' >I' "'l f j''''''
'j'-1l' .tnt-FWI!
1 Ll('.II1IJ\ "M'r\IO'"
S10NI..t H' nus 0
Anlf.' "l .'fl.II'l. lCCH tlllU¥IUII 011 SOllH"n.H
p..r r Il' cr ~ r ~ IP" "II
\ (". ( ,- .. '''.J
I j", 5/)) l~lI\~'I, : flp .~"u If'u , 1'111' !IIO"" (1fJU J/j) C-U!..ft
. "1101. VI~' ~I'" PlaT' ~1..lJC1l"l I tUIiD .' flll'll .
,n," T!," . "rU'LISII( : U", .,,,, "r.:(1S IHIOUC,ItOUI Hr;111011 .
II"F Ilh'",l)l''' ..' ..rs . .,...' "I..f 1..fr,Ut" PC_fS I
" 1', r t { . ~ , I "., ,.. (l ) ,., ~C 0111" "tl (\I', t.. J [I II a, ~ l' a lllill 't( Pit - f. a
,~, . '",.rl 'I I) ; ell" Io.'~' ''''U.I.H'
~ - ~ e .. ~ lo - '~I"'. )
(II'" ~/') (lI:liS"'II: . clH ~Hf" If.H . (111:' UOWIII (Ie'" ~/'n (-Ui"ft
~'\'" : "(.11 III.' cr'''\r f,nlalTC .,UUC'UII '''11111' 10
~,I,. ...r ..Pft" 'ftIIJ" :.uPUfllH rllJO' ; HIC.toTl' "'110 I fIU"l[ .
"'1',";("' - ",r"II~,q,( ; IU' ~I"t II:U01\ ""loo,"OU1 HC'llulII .
..,1' IU.IIP~ (.11101 I\l. JL:, "0:11" . II('III(alCUIOU\ (H(.l)
""\I,I','IH"II) I ~(L ~aHl' ~l'''!''''1 ,"'- M.40 (fjIl:CJI!1,,"Cl "lUf) ; Clf'.
.' ~ 1 ( nu", All'
',.. - ;'" C-. (lIJ - J<'I ''',)
"H' PO'''-'' (I'jH "/,) (IIL'I-cr ; .,,,, 5U,f' \41'" : C'III ".O_1it (1". J/J)
('U'..II' Jl!lBI ,.IU 'flll" HI',.:.(lJl~t 'tC'C" ST.UetuII I "'10
,oJ ,.tI . "O"~"(" . SlIr,ttl' rllS"C ; COIIIIIO" ,"., lOOT'
,.._rUrI',II" ..r>ilIF" : 'H, .''''1 TU!-'Jl'" ((PU,\:DU' ,n.(s 1 Ff'-
.'.'1 "'il"...'\r, f'I[,II.~t~ )1'" . H'- 5ur\10),f ,..C,-''''5 )l t.
.1~1".~"t' r.rj..,.~tr.1 P~Cl) (t"""":"'liIU<; . SHC"Clf'll'l'''. PH- ...
(I" 01, ,. l ,'lU.) ; C"H'I"t. \V' r "'1,,(. ~p,
.,' (oo. (J<; - -, 1'.)
fd '. n"," ~or...... (aU" 4IIlJ C'l'''H . \0'- . .,." D'" ..,'-), CIa,. l/l)
(.I'"IIf!, .11<,t . "'I "I, U"" 411') CIU5"H i 111111 1'1111)"" (I('u 1/)) CIUStotC
,"0' ; , IIlIfl'" \rJT l!C'" ~n" "'0"" (1-)'. 4/') 'IUHfF)
'~(' I> ,- fr"'otnl"<1 II:I"'latl~ - CII '''I(- I : .15'51Wt ; .....,
'1/tl . ',Uflll' '11(" . Sll(ttl' 'l'StiC . ff.. '11" IC01S
:'1' '''''('''1.11 ,.IIPI1(" ,JI!H' fl'" 'UrtUlPI' C('J,""U('US '0'(\ I
r .. Ir (I.'l" Sff' VI~' rIIU"~ I"'HI CftS'\ ,1II001-"fl' rFft'.fSCfll'
(..r.l) (""fJ'jLrr'l~ . SH"IIIl' Il"ll'" ,~. ".' ('IC""UIOl BlUf) r
',1'1 ,. r , (..01, I nL ~ '. 6. ,
~UI, j7. .q" o,'lll "..~ .l".~ (" ~, '-. ""!"'l. t'5 .{lSf '''LOW Ollf -f'fl. )i
... 1 "IJU'I " ...,,"r'51:J'" ro",,,,,,,,, uc,r,,~r '" t,tJPK'1I fO II:r t'U OF flit ')(.2. ,.."
ft~1 1~'1"1 II. H( II ~'. '''!ltC' CtSB I" h.( II " "foUI TO IIJt Ut efl"u. Ft
ll1"'~. 'I-' pJonfll1 1~ !.llr,!-Tl' fIlU"H1U~ 11 1\ ,-p. ....It..." "'tDICn, IIICt""
136
-------
Table A-2.
Laboratory analysis of Chinook-l soil.
S'JIl CLASSIFtCATlO"J-APl~lC HAPlC'I3DROLL
((,APSE-lOAMY, flUXc[j
-C~I NOOK
SE'IFS----
J. s. (ifPAcT"~NT OF AG"IC'JlTU"E
SOIL CLJNS'::~VATION SHVJC~, MTse
NATIONAL SOIL SUPyf't' lABOFATOPY
LJNCCJl~l, N';BQA$KA
SOIL NO -
S1b14T-087-1
COlJ~TY
pos E~JO
GF~ERAl METHOCS- - -114. lBlS, 2A1, 28
SAMPLI: "05. 76P0534-7bPC537
---- - ------------ --------------------------------- - - ---- - ---- -- ------- -- -- ---- ----- - -- -- -- -- ---- ---- ----- -- - ---- -- -- ----
DEPTH HORIZON c- - - - - - - - - PART tCtE S llE ANUYStS, L T 2~"" 36.1, 36.16., 36. lB - - tP AT 10
F tN~ 1 - - SANO - - - 1(- - -$ It T- - - -) FAMl I ~~ T P f Jt<.J[ '.JlJ~- 801
SA~IJ SILT CtU CLAY VCOS CQP S MEOS FNt S VFNS COSI FNS I VF SI T =XT !I CLAY crH- 15-
2- .05- L T L T 2- 1- .5- .25- .10- .05 .02 .005- $6."-1) .2- TO (LAY BA'
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C- (- - - - PeT LT 2MM - - - -) PCT PCT Cl AV
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B3CA
2A18
66.B
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20.7
18.6
26.2
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12.6
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3.4 43.b
3.9 45.8
3.5 45.5
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IAI
(B)
1 C)
fSTtMATI:
1:2 SOIL wAT~P !:.ATtO.
BY SOIL MECHMIICS LABORAT1f:Y, USD.&., LINeOl"!, 'IE.
137
-------
A1
82
83ca
II A 1b
Fig.
.~
.J
A-I.
Photograph of Chinook-l soil profile,
138
-------
Table A-3.
SI IL "~''':
(t . y., ., ~ rl! ".:
ll( t" .. f
(I" ~ \ J I- I' ~ I " " :
! '1 ~ ""'.: '
~t rrr: .
.10 Ii .ff ~H1J~1
Sf Il It ,..r IH'It~t
.1/'1:" Tt~ll"
P'tr !PT1AJlI q
PIli.' ~. Il IT' :
'jo' ~ II r.t 'rl', :
.. J( ~ I'~ rI " r I
VI fl1"fJr~t
"'11'" .lll "H:
"1"1''''
. ..
t. j;
. \J
. ..
, l'
, "
f ~..
F ~ ~
If.\
J("""
Pedon description of Boxwell-2 soil.
Sh"."U-l
" 1/-,
I. 1H l
'III ,/fI,. H II., \1''' lJ, HN, ""Ht ~ IInE5 "E 0' COLi"I', .,.
Sit PrIl,'IU
~U(."Gl' HC')'"
.eo. orGAffS r
nt(,ltfB F
':,.
HUlt leu 1013 IIEfU5 110"'" S"'LfD' 'UGU5!
_."fI. COIIVU .u'HTJ SOUTHWEST
lUII-tII: U nfe>UfS F "'NURI H OfCilHS F
SU'"U: IJf:GJfU F ,,'NUll. OEGUf$ f
"OllH r .UCU$T I: ,lrIoa file VltER UtiU
CIJJinOl Sfcun.. LIlitH -- U"fU 0.15 (It LOVU- 100 ell
()I'!Ula CLISS' "EU n...tUD
STOJiloUI( 55 I cuss 0
I'U"'.:
( 11\ ~ ..
u.'.U.\l1
"'''U.U:
,f p, ,~
'. coo.
~ ,"'11 j "E
,till u.t, 1.1'" IIIlL' ulIl'Jiles
"'I,;upr
,01\'). ~ -"r. . nil 1'1 5
'I ","l' ..U'HU(O If510UH ""f"H, lO(IL COLLUYlUiI all
,':TI~'tnrHII \''''o510M ...0 5"'U
SOLlFlU(U1f
'JI(.F1Lf C( sell.,110"
J - I c.. ( t - 0 I"'.)
"H' r",rf1~H flNO~~ (lvTII 41i) CJlUSHfO 1 lO" I un ou. !RealN (1091 2Il)
(~U:."IIJ .Ol!.' ; ~('" nt;, FIIII( ~"frlUl'" SfRuCfu.E I 5[F' .
,,1'''' r..I~"lf ,IIL"-SIICIY . Sl!f.I.TU 'LASTI( I ...., FIN' lOOTS
IJrq,,IJf,liUU1 IiOIUOli I ""U FIH ,UIIIUl'" (Oll1lllUOUS 'oafS I
.n'iCAlC~~HIIIS ("UI CO""frlUOUS I "OOfUlfl' HUlUIE ,.... I.l
rr'II'11"'.Ol "lUf) I ,lfl1l1,lI, 8(UhCU,
J - 1 c.. ( t. - 1 IN.)
'lIif" (Icn 411) CIU!.ttfO ; LOU I (JUII: 811~"" (10" ]11) CIUSttfO 'OIST
",rAr YfH' f-IPi( C,"A-'Ul,.1 STJlUCTUII( I sot, . WEI' FatJl!lf ,
'nP~"1'CU ,HIG"Tl' 'USTIC I 'U' FI"f "0015 'H"OU(;"OU' ..011l0N
fl..i 'UtllJllW CO"'UruOUS ,rJlf5 I IIIOIIICU(UfOU5 (HCl) (Oll1lIllUOUS
n',fOlrl" \l'AUht "'to. !.2 (~ItO"""ICL IIlUf) I 'lI8In..' IIOU"('"'
~ (.. ( 1 - "1'-.)
(lUU "']I CIU'..fC I lU. I 0'111: 11'011" Clna
...OUtR,n ..,,.( G"UUl'lI 5"UC1\1'l ; SLlGHtL' HUO
",Oll"l(n . nICO"'l' 'l'!IIIC ; '511' fl,,( .oOtS
-I"" "I"" IU8ULlR COt.JIIfUOUS 'Olll~ . "n"uLCUUUS
~n"fHlflf 'L.Ulld 'H- ~.l (UMO.,..'.n PLIIE) I U81"8..
11)) C'US..fO "OI5T
, ",If'"UHf
THUUGHOUT "0'110"
(HeLl CO'''''UOUS
flOUIIUU
,- )~' C". ( l - 4'''. )
",'.\0', U',u "'3J '"U'hle . H'" . 0,.., PIIC"'" (JOtl
VHH', HU ,,"..UIU S"U(.'U~£ I SLlr.HfL' HUO
."""01 1(" ,UIGt'1L' 'l'Stre 1 ~u,' ,.hf aODU
.,"" '1"[ TUeULJR CCI"'''''UOL5 '[If S ; "C"(ILea"fOU5
.,11'-1I1(l' .lUIIU"t ~h- 111.1 '''"O''H'~n HUJI-J I .11181"'"
JIJJ C'US"ft' aD 1ST
. un FUlfllf
I"'OUCHOU' "0'110"
(tI(l) CO"'IJlUO\iS
bOU"O'"'
I,' - ,~,' C-. ( of, - ~ ''''.)
"lll""-." \'11\1"" C1tfll "/<1) CilUS..ft I lOU I 0111' 81011" <10'" )/)) (JU!oHfO
""I" ~ "ur'.R'H ~f[lua U,HUUII !oTRUC'UI. I SLlGHfLY to"O ,
II"~III . 'iur,HTU HlCu , UIf,H'L' 'l'STlC I """ ftliof 'OOTS
I""I"II',I'OUI "ORIlC" ; IU,,", fUf IUUUL" CO,,",.UOUS ~O'fS
.'I...r~l(.&o('Otl~ ("(L) t:Oll""U'Jl'S 1 ""f'U"fL' 'LllALI"'f ~..... fI.l
~'~1"'It'..n PlLJ') . CUtl! !.r'1'" 110"'''0'''
~(- s" ["'. ( ~
I>w"" (lCu. 4/)
, ~Uc;'iq, 'CniT i
'JIII;oIt1' 'frpU"
, L I ! t' 'I' ~II [II:, .
rT..1'''' "'II" .
\ "( L) cr~l1 ",U'IUS
- .!io I".)
L$tIJSHlC ; sue' Cll? lO'" , V O' GU'UH !lIIO,,'" (lOT. JIl)
.tll oIfOIU" 'IIBIII"tC 0.' S1JIUC1U'f "'''''G 10
SIJ8A"r.t'l'lI I"lO(II:' I ¥fn ""0 . fill:. ,
-------
Table A-4.
Laboratory analyses of Boxwell-2.
SOIL CLASSIFICATlON-80ROLLIC CAM80RTHI0
FINE-lOAMY. "UEO
-Y'MAC
SEAIFS -
U. S. OEPARTMENT Of AGRICULTURE
SOIL CONSERVATION SERVICE, MISC
UTIONAL SOIL SURVEY LA80RATORY
LINCOLN, NE8RASKA
SOIL NO - - -
SI6MT-08l-2
COUNTY - -
ROSE8UO
SAMPLE NOS. 161'0538-16P05~9
GEJtER &l METHODS- - -lA. 1811, 211. 28
- --- -------------------------- --- --------------- ---------- ---------------------- -- ----- ---------- -------------
CM
SAND SILT
2- .05-
.05 .002
1- - -
- - - - - - - - PAfI:TlClE SIZE 4NALYSJS, LT 2"". 3'1, 3AlA. 3118
FINE I - - SAND - - - - - - 11- - -SILT- - - -I FAML INTR
CLAY CLAY VCOS CORS ME OS fNES VFNS COSI FNSI VFSI TEXT II
LT LT 2- 1- .5- .25- .10- .05 .02 .005- SANO .2-
.002 .0002 1 .5 .25 .10 .05 .02 .002 .002 2-.1 .02
- PCT L T 2MM - - - - - - - - - - - - - -I
- - IRATIO
F (NE NON- 801
CLAY C03- 15-
TO CLAY BAR
CLAY TO
PCT PCT CLAY
DFPTH
HDR 120N
1- - -
-- --------------- ----- --- --- -- ------------------ ------- --------------------- -- -- ---------------------------
000-001 All 48.T 36.~ 1~.9 .2 2.5 2.5 22.~ 21.1 24.3 12.1 21.6 15 .86
001-002 A12 ~8.9 39.1 12.1 .~ .5 1.6 23.1 23.3 25.5 13.6 25.6 12 .68
002-005 Al3 ~9.0 3T.9 13.1 .2 .~ 1.3 22.2 24.9 25.~ 12.5 24.1 13 .~~
OD5-0 10 Al4 ".1 31.6 13.3 .1 .~ I.~ 23.3 23.9 24.4 13.2 25.2 13 .~3
010-022 Al5 46.9 33.8 19.3 .1 .2 1.1 22.3 23.2 23.5 10.3 23.1 19 .31
022-038 821 48.1 31.0 20.3 TR .2 1.1 23.8 23.6 21.1 9.9 25.1 20 .~1
038-050 822 49.3 30.9 19.8 .1 .1 .9 22.5 25.1 20.9 10.0 23.6 20 .~O
050-060 823 47.1 33.2 19.1 .1 .1 .8 19.4 26.1 22.9 10.3 20.~ 20 .~I
060-015 UCA 38.1 35.3 26.6 TR .I .6 12.8 24.6 24.3 11.0 13.5 20 .35
015-100 C1CA 42.3 34.9 22.8 TR .1 .3 11.5 30.4 22.0 12.9 11.9 11 .36
100-145 C2 ~6.3 34. T 19.0 .0 .1 .3 13.3 32.6 21.9 12.8 13.1 19 .38
000- 005 1&1
------------------ ---- ------------------------- ---- -- ----- ---------- ----- ----- --- --- ----------------- -- ----------
CM
(PARTJCLF SIZE 'NALYSIS. MM. 38. 381. J821C eULk DENSITY
VOL. C- - - - - - - WEIGHT - - - - - - -t 'tAIO 4AIH 'tDi
GT GT 15-20 20-5 5-2 LT 20-2 1/3- OVEN COLE
2 15 .01~ PCT 8U ORY
PCT PCT 1- - - PCT LT 15 - - - 1 L120 G/CC GICC
'1- - - -WATEA CONTENT-
~81C ~81e ~82 4P
1/10 1/3- 15- WRD
e'R 8AR eAR 'M'
PCI PCT PCT CM
- - -I
CAR 80NATE
6El8 3&lA
L T LT
2 .002
PCT PCT
1- -PH - -I
8ClA 8CIE
III 1/2
H20 eAtL
DEPTH
- - ----------- ----------- --- ---------------------- ----- ------------------------- -- -------------- -------- - ----
000-001 n 0 0 TR n n 1.1 8 12.8 1.0 6.3
D01-002 TP 0 0 TR n TP 1.1 8 8.1 6.5 5.9
002-005 n 0 0 TR TR TR 1.1 8 5.8 6.3 5.6
005-010 n 0 0 10 TR TR 1.2 8 5.1 6.2 5.6
010-022 TP 0 0 0 TR TR 1.~3 1.48 .003 14.1 1.4 .10 6.~ 5.9
022-038 TR 0 0 T. TR TR 1.59 1.61 .012 16.8 8.4 .13 6.6 6.1
031-050 0 0 0 0 0 0 1.9 n 6.9 6.3
050-060 0 0 0 0 0 0 8.1 3 8.0 1.5
060-D 15 0 0 0 0 0 0 1.62 1.11 .028 14.2 9.3 .08 18 8.4 1.9
015-IDO 0 0 0 0 0 0 8.2 21 8.6 8.1
100-1~5 0 0 0 0 0 D 1.48 1.61 .D28 19.~ 1.2 .18 15 8.1 8.1
000-005 1.10 1.23 .040 21.3
- - -- ------------------------------------------------ ---- --- ------- ----- --- ------- - --- -- ------ --------- ------ ----
Of'T" t DRGANIC MA TTfA I JAON PHOS 1- -EXTRACTA8LE 8&5 ES 584&- -I ACIY AL lCAT EXCHI RATIO RATIO CA leASE SAT I
6AU 681& CIN 6C28 6N2E 6020 "28 6Q28 6HiA 6G1E 5A3A 5AAR 801 803 5F1 5C3 5C1
OAGN HUG EXT Ton CA MG NA X SUM 8ACL xn EXT8 NHAt NHAC CA SAT EXT8 NHAt
CUI FE Exre TEA EXT ACIY TO TO NHAC ACTV
C. PCT PCT "T PCT 1- - - - - - - - - - -MEQ I 100 G- - - - - - - - - - I CLAY MG PCT peT PCT
--------------------------------------------------------------------------------------------------------------
000-001 3.41 .316 9 13.1 ~.~ TR 1.4 1~.5 5.0 2~. 5 18.2 1.22 3.1 15 80 101
001-002 2.32 .201 11 1.2 2.9 .0 1.0 12.1 ~.3 16.4 13.5 1.12 2.8 61 1~ 90
002-005 1.30 .118 11 5.8 2.2 .0 .1 8.1 3.4 12.1 10.5 .80 2.6 55 12 83
005-010 1.14 .106 11 6.1 2.1 .0 .1 9.5 3.2 12.1 11.0 .83 3.2 61 15 8A
DIo-022 .88 .089 10 1.2 3.2 .0 .8 12.2 2.9 15.1 14.0 .13 2.6 59 81 81
022-038 .66 .011 9 8.1 ~.~ .0 .5 13.0 2.6 15.6 15.~ .16 1.8 53 83 8~
038-050 .56 .063 9 8.1 5.3 .0 .0 13.~ 1.9 15.3 14.1 .1~ 1.5 55 88 91
050-06D .51 .010 8 1.5 .0 .~ 13.9 .11
060-D15 .40 .046 9 8.9 .0 .4 11.D .41
015-100 .25 .029 9 13.8 .0 .3 10.1 .44
100-145 .22 .022 10 11.1 .1 .3 10.6 .56
000-005
- ---- -------------------------------------------------- ---- ---------- - ------- ------------------------ ----
OfPTH C5ATURUEO PASTE I NA NA SALT GYP 1- - - - - - SATURA TI ON ExT..cr 8A1- - - - - - 1 ATTER8ERG
8El 8C 18 8& 502 5E 805 6FLA 8AlA 6N18 6018 6P18 6Q18 61lA 6JlA 6X1C 6LlC 6MIC 4Fl H2
REST PH H20 ESP SAP TOIL EC CA MG NA . C03 HC03 CL SO~ N03 LQI D PLST
OH"- SOLU MIIIt051 LMIT I NOX
CM CM PCT PCT PPM PCT CM I - - - - - MEQ I LITER - - - - - - - - 1 PCT
--------------------------------------------------------------------------------------------------------------
000-001 6.~ 15.0 1000 1.11 11.5 T.3 .1 2.3 .0 16.8 .5 .8 .0
001-002 .10C
002-005 .10C
005-010 .10C
010-022 .10C
022-038 .10C 28 9 0
0"-050 .10C
050-060 .20C
060-015 .20C
015-100 3900 8.4 .20C
100-145 3100 8.3 39.2 100 .36 .6 2.1 1.0 .1 .u 2.' .1 .5 .1 28 9 0
00D-005
;~ ~- ~~~ -~; -~~ ~~ -~~~:-~;~ ~~;-;;-;;; -~;~;~;;~~-;~~ ~~;;-;; ~;;;~~:------ -------- - ----- -- --- ------ ---------- ----
(II eST1..ATE.
CCI 112 SOIL WATe" RAT10.
(D. IY SOJl MECHAHICS l&80RATOJl:Y. USDA. LINCOlN. HE.
140
-------
A11
A12~
A13-
A14
A15
821
822
823
83ca
C1ca
C2
j ~~ IL .
, ...!'. J'
. .;' / '- . '. ',.'.' ,~'.!.i.,
I ' ! . '. -i ,~' ~.
'Ii' , i:': ;1) :-~" ... ,';:,,:;
.' .1'\ ",' ,. , . "''', ,..."r..,./.,..,
I' ".1 t . / ,.;,' , 4"1.':';'" \ . V N;.' ""~ ,'~" ~ \'
.' .,' .,I',.jI, .' /,,"",' I .,,-. .' , ',. ., '
. .,/ " .".".,( ...,' ,.. . .. ",
; < J' :1}< ..,~~~1~):if ~. ',.of. ~ / ! . I;" ,,'
~L / ..'f.,,..1 .',: < ,:~. " ...\\-...~-'''f''..' " ,/A
t' .," ,';p,- , 'fj!/"""" ,'1 . ..' .."';" I" '
..""..;. ,'" ,./), . " ./ i ,.'iJ;f,." iX,,'. . . I
t},"'~i( '. ;. .' ,;W ,,":.I~,:ii~,'~\~}t,"'I:,'i r
.'.' .,' .,",.';". '''''.)' .,' ,!.,~;;,:~~{~';lNi'Jf:~~~:~">'<'
.' '. " ..' " .i " .;.. ~. """"'".,r, ,-;':'. "'."'~
., ,.(,. ,~"., .,' ' '
-------
Table A-5.
!£T l ~l' I' ..
~t t ~" . r . r l' ",.:
trrn'r.'
(I. . ~' " I (., I r..:
\!11 "".
HN'" ,
.111 1 -!'.'llJ"'
\r It 1'. r' , . ,,'~,
"'11- ""ll'
,He !+'~ In!':
""""ll'-:
,~, < I, r , I ~... .
_f ',,' , ., I ( ~ :
,..,., ""."(:
. ..
. I.
Pedon description of 1948-3 soil.
l\~' ","U\
to ., ~.
'\01 ./40. " J/". \1(1
I) 11 j J
". T.'. ..0,1'. I " f'S' i" (111.\'. '" .,
I'll' r I. \. I ~ ( " \.. \
'l'"'' ",.t' \1'1'.
'.., '."If"
','I",: ,
'f!':
tLt.,,"Cht n""1 "tJt~s "0"'" SU'ltDI .~'u"
IUCI PUfrof A\'''YI
\U'''f't 't ()~Oll\ r WIIIUtl .<11 rf,UE\'
H'ufQ: "",(lffS' ","nll nF,IfIS"
-n."" '\1""\' &'",D' fro' ""'ft, '"ILf
,-orHI 'HUICh lflilltS .- U"fPl Ol~ C" LOWU1 ue e'
{..'HArf U"'S51 lULL O.&IIII'D
'TO"I"'S! I (lISS 0
~r ~.I'J"1 ("'II) [r..tl'I'n,', I 1II1"f)"."l' 'L"lllllf .... I."
,.'f ~, '~Il '11") ; ~r Li>I ~~'" 'rlJ~r~~,
~. ,,' ~, (.t .. I,".)
,.t,,',. (I ,. '/.1 L~L\tfr I l'~~ : (.HfI ""'\'" ".C~, (1(," "l)
."'J' 'I ~,..y ; ~IC' Ptl~ ~~fr.... (It'P ".., (PLO..IL I It. ""ll"I!;H "0111111
I.'~ ,,.), ~"'.' I [ 't 1'1 0 d PI "LI',I ,.8.r '1l I lCIIil wr., (.'1: c..'"
\1.' " '"" ".., !,e' I ("O~ (r',n~'",.. .ITI~!~l(~ - C. '''ICII I .
\1" ~, .. V'" (, t J ~ f 'L "' Shill II f( ; \11 T ,y(., (1I1"l' ,
,r'.II'Of ,\I!fHt' "16~'1( ; 811\' 'I'" 11100" ,..rOLU.OU' ..n'lle",
, :Hf(i,lo, ~',..t ~ : Vlvll"'" ffFt"~UCf~' (HeLl eOllftlllueU!.
."'1' ~t,I'['q 1'..- ",' "w,.1""'(L "l'n) . 1"1"'" .OUIIC,II,
1 . '. l.~ (.. .) 1".)
"p',,'," H.... f! ,. ,I,') LWl'Hl ; l,lt. i 0.,. rill'tS'" 'flO~'" l.O" .,1)
'''I''> I .., 1',1 ,VI"' "'It ~~r..... LI',', 7''', C"U"H'C I L'. "lL(,~IS" "0.l1li
1.-") (Cl"" 1 .::" 0 tr'.,,"" .' f "J' l ((.'\1 '.0111'1(""
"'~..1 ' " Ll . (h'" ".) (-U',."'t .r1ftl ~ ; .tf II'f.C''''' ""'0 ~llT le'.
, . .'S' II'" J/d LOl~~'( r~jlO(I'I~L .&IIIIO!. O. - till ,..,e-) . ""5!IVf .
t' ..,IL~ "",1'-, ,'I" r"I~"lt I ~'I,'1T(fI' . 5LIC,HTL' 'llSlle ; JOt..
',' ~tl", r...'I'I".,,,, ''1I>I/P, ; .,,,, f''''f I-R'GULA' ,e'f..
. I I' ',I '.' ., t '.1 ,,('..1 ('.tl) (f..' [.t.r'l.J\ , "rCf',UL' "LIIll"t ,... .~.
. r . l' ',"' t "I.r) ; t ~,' 1 T ~: L, , III [ ~P'
- \oW. (l'- - ,'II".J
If , .". 1 ,,~, (Il'" '/I) ("li'.oH' ; Lr,~. : "LtCI (10'" ~/I) C'U"".O
""1 IT. "UIIoIS" ~~I'"" (1"" ~n) 1"<11[11' . 'lllL"I.... .'C"III (10" ~/4)
.1,.' 'It. T ; Ln,,,...,, '.(TvO f. LIH:,t ""'1"'''' !'C""'U" 'fllO.
'.' On) CIIU\HrC ''''TIt', . ;.. pr"(r,,,' "'~'1 Sh.' l'}llII ~f" tl" C..,'
f: ". 'I) (~"',~If lI"".~('l "",f< ", - '"~ "qC') I .'''!.J~' I
LIE "I' ..~11"" !I"lJWC'"
. l).. ,'I, I J" - , ~ I' w)
I To 'Ill .' ,," '.'."~ L'.~' ~"'J (lIl\..,C ; I". . llC,,,,' ttllY' ''10''. (l.~' ~/4J
-~!/,,'U'J .,-nl ~"n.. ,~"'"" l'.'1 ~'n C'US~'O I 01111 "."U" "'OW.
ll..~' HI) (.II'U\"'[ "fl\1 0 (f"'I. '-(1""" cr&rH '.0"'.111'
,... ..~I'" "Ll'1oI L," "., (~lI5"'Cr 'fPI"'" , ,L PfQCUIt H".O SILl l('"
ir;, ' - ~~, '1' ,'- "') I ~u",",( '-,"''"(''6l "6"f,~ r# . ,. '''''II) I .'SSIWf I
~II 1(' ,~.! I ~'" ~"I~~lf . 'ur'"'t' "1(-' . Sl"hTlY'll..'IC I
" " ',"T~ 1"~"O,;(.~"Jt "1"lr~ ,"''''' I"'. l"UGUl" 'O"S . ff"
>Itl ,q(,~f,1' >; (II' 0 -If'~.II' IFrr.'u',(t",1 l"CLJ (O"II..UnU!. .
.'f'lt-rlll' rL'.,II" r.- "o~ \'~i'I,"'''(l ~lvf) ; tdT 'f.eHtD IIlnUfIIO'"
'" I' 6, " I' 6. ~ ~ I' 6. Sf (, J ~, 1.'. .." I'
,I>' .' I'of '.., 11<," C'..,'I-r., '(""'1 "IUVll'C '" 194111 J(I COU." 1(le CC"'U'U
,T1'.o /11,.- II, 1~7" . '!l 1 ~p .,.,~ ( ., ~- (., U'.l ""SColllf"'5 1111 COIIIIO. ,....
U" . " T .:1" r r l. : ~. 'tr .0" (J{ ,: " 1 JoL 15'», L,.P(,I' , ,I.GIII "" Of S"'lt I"tC"
"'I,. "I, "t'ro. ',I.\lrl',1 .A"~Ul I\V'(I.,t:r "'I'" COil ""CtOt"".. ....S eflL
n., 1 ~. "I-. '111' :'(J ~~! 1( ('~.I',' 1'1 ',1fT CI1Il '(;(.f'5'1 IIC CtO. ,..,
.~..-." T... '~'Il," .,11'~'
-------
Table A-6.
Laboratory analyses of 1948-3 soil.
SOIL CLASSIFICATION-
SF'IFS -
- - -MIN' SPOIL
J. s. (J~PIlRTMfNT OF AGPICUlTURE
SOIL CONS~j;VATION SERVICE, MTSC
~ATIQNAl SClIL SUPvEY lABO~ATORY
lINCOLN, Nt"BRASKA
SOIL NO - -
S76MT-087-3
C~UNTY
P,QS ~8UD
:;eNF=p Al METHODS- ... -lA, 1818, 2Al, 28
SAMPLE 'OS. 76P0550-76P0557
... -- -- --- -----... ---- -- -------- ----- ---... ---- ------ --- ---- ---- - - ---... -- ------ - --- --- --- - - -- -- ------ - -- -... ----... -- -- -... --...... --
OEPTH HOR IlON 1- - - - - - ... - - PAFTICLE S lIE ANALYSt 5, LT 214119, 3Al, 3414, 3418 ... - - )FATIO
F (HI; 1 - - SAND - - - 11- - -SIL T- - - - 1 FAML I~TP F (NE PIIC"'- 801
SAND SILT CLAY CLAY VCOS COP S MEOS FNf S YF-NS COSt F NSI YFSI T~XT II CLAY C03- 15-
2- .05- l T L T 2- 1- .5- .25- .10- .05 .02 .005- SAND .2- TO CLAY BA'
.05 .002 .002 .0002 I .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
CM 1- - - ... PCT LT 2MM - - - -, PCT PCT (lAY
-- - -- ----- ---- --- --- --... --- ---- --... ----- --------- --------- -- ----- -----... -- --- -- ----- --- - ---...... - --- -... - - - --... -- -... ----- -- --......
~OO-OOI AlI 48.6 37.6 13.8 1.4 1.4 2.2 26.3 17.3 19.8 11.8 31.3 .B7
001-002 Al2 51.1 35.2 13.7 1.3 1.9 2.7 28.1 17.1 16.3 lB. q 34.0 .64
002-005 413 45.4 36.1t 18.2 .6 1.1 2.1 27.3 14.3 17.9 IB.5 31.1 .4T
005-010 C1 49.9 34.5 15.6 1.2 .9 1.8 31.0 15.0 18.4 16.1 34.9 .55
010-050 C2 45.q 36.8 17.3 .5 1.0 1.9 28.6 13.9 IB.5 18.3 32.0 .13
~5()-1 00 C3 55.0 31.7 13.3 .6 .8 2.2 34.8 16.6 17.0 l4.7 38.4 1.00
100-153' C4 32.7 48.1 19.2 .9 .3 1.0 13.7 16.8 24.9 23.2 15.9 .b9
COAL
---- - ----- ------- -------------------------- ---- ------- ------ ------------ - ---- ------ - -- -- -- -- ----- - -------- - --- - - -- ----
'EPTH
C-
IPA'HIClc SIZF MJALYSIS, MM, 38, 381, 382ft BULK rENSlTV
V(lL. 1- - - W;:IGHT - - - - - - -I 4410 4A1H "01
r.T GT 75-20 20-5 5-2 IT 20-2 1/3- OVEN COLE
2 75 .074 PCT BAP OPY
PCT PCT (- - - PCT IT 75 - - - I lT20 G/CC G/CC
11- - -
'tBlC
1/10
BU
PCT
-wATE!" CQNTF;NT-
48 Ie 1,>82 4(1
1/3- 15- WPO
BAR SAP CMI
PCT PCT C'"
- J C f4HWNA TE
6:18 3AIA
L T l T
2 .002
PC T PC T
(- - PI-t - -.
BClA BCIE
III HZ
H20 (ACt
- - - -- - --- - -- - - --- -- -- - - --- -- ---- ------ ------ - ---- ----- - - -- - - - - - --- - -- ---- - - - -- ----- --- ---- - - - - -- - - - - --- - - -- -- - -- - - - - - - --
000-001 3 0 0 2 3 5 1.2 A 12.0 7 T.6 7.3
001-002 5 0 TP 4 5 9 1.3 A 8. B 8 7.7 7.4
002-005 8 0 2 7 3 10 1.55 1.62 .014 18.1 8.6 .14 9 7.9 T.2
0~5-010 10 0 0 7 9 16 1.70 1.74 .007 15. B 8.6 .11 12 8.0 7.4
010-050 9 0 0 7 9 16 1.40 1.44 .009 20.4 12. b .10 II 7.6 7.3
05()-100 12 0 0 11 12 23 1.3 A 13.3 10 7.5 7.3
100-153 6 0 0 B 6 14 1.19 1.25 .016 24.0 13.3 .12 9 7.6 7.2
1.21 6.0 5.8
- - --- -------------- - ---- -- - - -- ------- --------- ------- -- ----- ----------- - -- ------ - -- -- --- -- --- -- - - -- ---- - ---- - --- ----
DEPTH IO"G4NIC MATTf" 1 IP.ON PHOS 1- -EXTPACT6BLE ~ASE S 584A- -I ACTV Al I CAT EXCI-t) ~ AT 10 PAT IQ CA (eAS[ SA T J
6AU 681A C/N 6C2B 6N2!: 6020 6P28 602B 6HlA bG 1~ 5A3;\ 5Ab&. BOI 8C3 5F 1 50 5C 1
f)RGN Nl rr. FXT TOfl CA 'IG NA K SUM BACL KCl EXT e "'IHAC ~HA(. CA SAT f XTB NHAC
CAPB FE E XT8 TE4 EXT AC TV TO TO NHA(. ACTV
C- .CT PCT PCT PCT (- - - -MEO I 100 G- 1 CLAV "e PCT PCT PC T
- - -- - -- ----- ---------- ---- ------ ----- - ----- - - -- - - -- - - --- - - ---- - -- - --- - -- -- - - - - ---- - - -- - - -- - - -- -- - - -'-- - - -- - - - - - - - - - -- --
000-001 ~.ll .333 15 8.2 TR 1.2 24.9 1.8J
001-002 5.0 I .213 Z4 8.4 TP .B 22.8 1.66
002- 005 4.16 .145 29 9.5 TR .6 21.9 1.20
005-010 2.83 .092 31 10.9 .3 .6 17.7 1.13
010-050 5.94 .129 46 16.2 1.1 .2 30.5 1.76
05()-100 5.52 .131 42 21.2 .6 .2 34.0 2.57
100-153 5.28 .131 40 19.4 .1 .2 ]q.5 1.77
13.0B .959 14 .OC 15.2C .OF
------------- ------------ -------------------------- ---- -- ----- --- ---------- - - -- -- - - -- ------ -- ------- ---- -- - ---------- --
DEPTH I SATUCUTED PAS TEl NA NA SALT GYP 1- - - SATUPATlml EXTR ACT BAl- - - 1 ATTERB[PG
Be I 8C IB SA 502 5E B05 6F lA 8AlA 6"B 6J 18 6P 18 60lB 6116 bJIA bK 1( bUC b~lC 4FI 4F2
AF.~T PH H20 ESP SA~ TOTL EC CA MG NA K C03 HC03 CL S04 N03 lOll) Pl S T
OHH- SOlU "MHOSI l'1l T INOX
CM CM PCT PCT .PM PCT CM ( M-:O I l t TEP ) PCT
----- -- -- - -- - ---- -- -- - --- - -- - - -- --- - -- -------- --- - -- -- -- ----- -- ------- - - -- - -- - - --- - - - -- -- -- -- -- -- - - -- - -- - - - - -- - -- - - - - --
000- 001 6.8 63.2 2000 0 3.B3 29.1 15.1 .6 ~.6 .0 3.B 3.9 3.2 .0
001-002 7.5 43.2 620 1.80 14.0 6.3 .2 1.9 .0 14.1 2.5 1.4 .0
002-005 7.5 41.0 420 1.31 9.3 4.9 .7 1.1 .0 10.t 1.4 1.5 .0
005- 0 I 0 7.6 40.0 430 1.47 6.7 ..8 4.2 1.0 .0 5. I 4.2 5.8 .0
01 0-~50 7.2 40.9 1100 3.48 14.6 12.4 13.5 ' .~ 3.5 19.1 21.2 .0
05()-IOO B30 7.1 41.3 1900 4.96 29.9 31.3 8.7 .2 .0 2.5 28.6 38.1 .0
100-153 2200 7.3 43.7 510 1.51 7.9 8.8 1.4 .1 .0 3.5 3.9 9.6 .0
5.9 122.0 1000 1.11 4.4 6.6 2.0 .2 .0 5.3 1.0 3.9 H
- - --- --------- --- ---- - - -- - -- - - -- --- - -- -- -- ----- - ---- ---- ---- - - --- -- - --- - --- --- - -- -- --- -- - - - - -- - - - - - -- -- -- - - - - - - - - - -- --
( AI
'8 I
I CI
101
1 F)
ESTIMATE
ORGA~tC CAR8Of~ Fe'P COAL SAMPLE ON <0.25 111M HATEPUl . 35...
FF FOR THE <0.25 101M MAT(PIAl . 0 PERCfNT.
ACtOITY FOR THE <0.25 MM MATERIAL .. 31.1 MC:Q PER 100 G.
At FI'JA THF <0.25 ""1 IIIATERtAl .. 0 PERCENT.
PHCENT AND 0"1 Hi~ <0.002 M~ MATfCllAl ; 37.0 PEPCUiT.
143
-------
A11~
A12-
A13~
C1--
C2
C3
C4
,f -..... \
,..
t.
. ,).
Fig. A-3.
Photograph of 1948-3 soil profile.
144
-------
Table A-7.
Sfli \1. I
SUPVI' ~'''I>l' "'.:
tH'T ro~:
(l'!I!:dr 1(' III' :
5 I If "1.: 1100 ..
SLnpt I 4
"$I lo'r",~Il'~'
srlllf""-"'Ii'l
Io'f.. tll(':
,~ I ( I.. 11/1' ..:
"I>, I ... II ,,,:
'~'HI'O~'" ,:
.. , ( ~ 0' ~ , l I ~ I :
'1".""'"...:
.. 'I!' .., . rJ ' ~ I,} I :
101:"'1.'1/",
. II
. I.
, ,
la'
l liT
. l'
Pedon description of Ethridge-4 soil.
tH,IIJfH.1
SH!Ml 11 j ...
...., 114, ~r It4. H 114, Sf(T 1 TJfrj, $141" } "'I Sf Cf (I')LSTMIP. 111.
~.Tr It 81t~.Jl'w~nLS. fU~. '(,,'IoCIIIlU,""lC
tnll'1';
U\V," ,.. 'Ill' lfv'l
",'".\l: lot n,r,IeIIS'
..... '111 : {1t I,ll L f" ~
"r"I...: C80
. ~ l'.
"'I'll '~1Il' ~l 'II-
L\ 1"<;, I It. It Tall tJld "t.Gl
, '" HI'''' '"', Pt rll, ~., If"
',PA ""', "11 Hl"~S "..r ""IIU""
,1I"..'!, II'f.5"'"11"[ "f!.TnU't ."H'IH, lOCH (CllU..lulI 01
Ulr.'.quI/S "htol' "rJIIII'",.Ul
(\tV'THIII; lCt, "'fUll! 1110.014 SU'PUt': 'UGuS1
';''"01 (OhWfl ASPfUI flOQ,HUSI
SU,II1P: ,,, "(t,H(!. f ""'H': t4 DEtHES f
Su.."t.: :JH,~ff~ f W''''HR: DftR((S F
"("110: rIlC'J~' 1:,,,,[': H ""'HI UPlf
(fJ"'Pl1l srcTJO" lIlIIl'S -- U'Hlt 010 C" lOWER: OH C.
[ltiUtt naH: wHl 011 "'IUD
STOIIII~fSSt cuss 0
SOlHlU(UH
PIICfllt 0' St:~ I."IH.
J - 1 lll. ( ~ - . II".)
~6LI 1.f1.." O:Jh un (lIl,(t,UCU~ : "cr'I'1rl' At'HI'" "H- 8.' (pfn'Ik'''')l !'lUF)
H"".t.., I(,U"V.'"
(oil.. ( 1 - ~ r..)
rAt~ "prr",~ (1..rYl- ~/') (ItUSttIt" (tA' In,.,. ; fJIOW!II (1'.'11 4/J) (PUSt-fe
"I""A,,( STlilt(IU,I
'"Ij~ "',,' U l' ~ fll 1"(11: T ; I' APf' . f I Ii III
.. ~ ", , , t f ~ f (' , ,~" nll(,.."UT "'1"111 ["
t> 11" " ; ~ ~ P r .. C j ~ 1 " I " , { l t' ~.. I '" "
PiCtJ t:"""'HJ.1I,", : ..r'lHp'''l'llrll.ll''
""I[I'H' r-nultjO.\r..,
; 'HU,"" (10.. 41l} (IIU~HH "OIH
PtPTI"<, If SIIIOIII', FI"'F l "rCTu..
, SIICIO . Yfll' PlaS1IC ;
; 11\&'" f IlilF IV"Ultl (0,,"THtln!..5
r.. Pt[ fHt5 ; r.O"(H(UfCUS
PH- 11.( (IIPr..,,,,,.ol All!f) I (t( I'
"J - .1 (.. ( 1 - It 1,,".)
IIn to, (I{,'P "'.') OI;S"'l . ~ Il" Cl~.
'I'!)'I!1f rl~£ Plln"~'lC -:;'()tJ('U~1
,HI t..rUl H Dln(., ; "a!ln ,~I."
( 'I"" ,~ f I" l II: (J 0' \ tt I 10 f f" .., C "
I' If. '0 ; lll.""" ,a J" 1 t.l .., ~ J.I" ~
(1'1'" 1 1'.. LJ 1 II ~ ,,,nr,' II ~ tr t' Al' all OJ' P,..-
; "'(.10'\0
P~H I"C. TC
. \'H'"
. "l'" ~ ,,, f
lo" p'r r AU!
D.I : Clf'"
(10,. "'JJ (Jlu5Hrn "ulS!
5TAOfilr. ""'f (. .~OJU"
, HII' "llHI( I
IU"VlIII «(''''''I''lOUo;
I IIjt')NOlC""fCUS (H(LJ
lilY. 80UIII(U,
, I - < ~ (10. (1- - .l; 1'\0.)
~I. ,'Ul'wlS,.. ~"CII' f\uH tH) (PlS"'f{ : SILT' lln ~C... ;
l.~'~ ~,~) I..IIU5HC -115' ; w"" Y~" (nil/Sf PPI5",aQC
?r" 'T IP,,, ,,.., "()')f" Ilf ~, ~ t V. ~UP 4"", Ut A II "l ((" : '" "g C
',TIC.' . Pl4S11C : ("-I" r1H ~'JLJ<. t"tn..." PfOS
'tr~.tlH (.2"~"'U'1U" r'I~'~ : (n"""" f'I"" (I" \.,..S
I'" "crl (,..t"".rt~ ~"I'I.. P'"IS ; "fU~~1Il' fHtll\'t\Cf"I l'i(l}
, '" ">,' t, !rot' ~t ! ... I r-o - ", {Io~ I'" T ~,. (t r'( ut ) I'," Af}U'l Sill 0 OlH
HllC",5,.. "'0"'"
~TPu( IUPf
. eu.
; ~ a""
Fh(
(1)10" IIjl.tlUS
'ICU"'DU'
.' - 1.... L". (t( - j'l I...)
tt~' PAll PPIJW,," (I"". JJl) (IiUSHt : SIL" (In t(J" : HllOIIIS" 'lI(.ljP" 00"'- ~14)
(wlI'r-olf, ",I'1H' . 'lot", y,,,, (C,..~: "lIr~.aTl( f,TIIU(TURE ""IIt.(; TIl IIf"
Into' "'tJ~A'(;UllII ur(.., : I-Hr . filll"LI . SlI(H'l' sue.. . 'l'SflC t
"'W.1Q !lVOTS f!fTWlr" ptr.. ; (I}"..n" Tt' "H.' fl"'f fV8UlU COt.UIiIVDIJS
",P'~ . q", 'AI"" (la' "".~'.' "1"1 fU'IIlH (l"1IHJU..~ pr;..I" . 'OOfIU£l' FJ'tIYfSC('"
("'(t' (r,,'".unUS , 51~I'"rt' "'.. IL ,,,[ "t"- ~.r (f~r,""'"Ol !'le£) ~
\ ,11 1'" (I"!J I l'fI'fjll.~'
'u.. IJ, ."1' 5',a
11,1 f. 101-11,"',
Iru '...' ( II ~. (.. (,"',lJ" ("SlAlS ll",r Sr,,( I'. \'OIOS 1111
145
-------
Table A-B.
Laboratory analyses of Ethridge-4
soil.
SOIL ClASSIFICUIOH-APIDIC ARGI80'OLL
FIHe. MOHTMORILlOHJTIC
SERI'=S - - - - - - -ETH~tOGE
~. S. DEPA.TMeNT OF AGRIC~l TURe
SOIL CONSERVATION seRVIce. MTSC
NOT IDNAl SOIL su.vev lA80RATDRV
lINCOlN. Ne8'ASKA
SOH Nr:1 - - - - - - 576/14T-087-4
COUNTY
ROH8UD
SAMPle NOS. 761'D558-76P0561
GE~ERAl Mf:THOOS- - -IA. 1818. 2At. 28
---------------------------------------------------------------------------------------------------------------------
oePTH liaR1 ZON 1- PAPTICl" SIZE ANAL VS I S. LT 2"M. 3&1, 3A1'. 3A18 - - - !PATIO
FIN! 1 - - SAND - - - 11- - -SILT- - - -I FAMl INTR FINe NON- 801
SANO SILT CLAY CLAY VCOS CDRS MEOS FNes VFNS COSI FNSI VFSI TeXT II CLAY C03- 15-
2- .05- 1 T 1 T 2- 1- .5- .25- .10- .05 .02 .005- SANO .2- TO CLAY 8AR
.05 .002 .002 .0002 1 .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
C. 1- - - - PCT IT 2M" - - - - - - - - - - - -I PCT PCT CLAY
-- ---- ----------- ------ -- --- - -- ---- -------- ------------ ------- ---- ------------------- ----- ------- ------ ---------------
000-001 All 28.9 ~8. 2 22.9 .5 .3 1.0 12.2 1~.9 23.8 2~.~ 1~.0 .40
nal-002 A12 21.6 46.1 26.3 .1 .3 .9 12.0 1~. 3 22.5 23.6 13.3 .45
002-005 Al3 24.9 41.1 33.5 .3 .~ .8 10.8 12.5 20.5 21.2 12.3 .25
005-010 Al4 22.1 )9." 38.3 .1 .2 .5 9.1 12.2 19.3 20.3 9.9 .25
010-019 82IT 18.3 42.1 39.0 .1 .1 .3 6.5 11.3 2a.~ 22.3 7.0 .26
019-031 822T 20.1 ~6. 7 32.6 .1 .2 .6 1.6 12.2 21.9 2~.8 8.5 .38
031-050 823 21.2 47.4 31.4 .1 .3 .6 8.1 12.1 20.1 21.3 9.1 .33
050-100 83 28.5 ~1.a 20.5 .1 .1 .1 11.8 15.8 20.3 26.7 12.1 .38
100-152 Cl 51.fJ 21.8 1". '3 .~ .~ 1.6 32.2 23.3 1~.5 13.3 34.6 .38
000-005 141
-------- -- - - - - - --- -- - --- ---- -- -- ---- ------ -- - -- -- - - --- - -- -- -- ---------- ----- ----- --- - ---- ------ - ------------- -------
r'lE PTI1
C"
(PA~TtCLE SIZE AN'LYSIS. "'H, 38. 381. 3B2)( BULK OENSITV
VOL. 1- - - WfIG~T - - - - - - -I 4A1D ~A1H ~Dl
GT GT 75-20 20-5 5-2 l T 20-2 113- oveN COle
2 75 . or. PCT BAR DRV
PCT PCT 1- - - PCT IT 75 - - - 1 lT20 GteC Gtec
I{- - -
H1C
1110
BAR
PCT
-WAT~R C~NTENT-
~B1C ~B2 ~Cl
113- 15- W'O
8A' 8AR CMI
PC7 PCT CM
- - -I
C~R8CNATf
6El8 3AlA
L T LT
2 .OD2
PCT PCT
(- -PH - -I
8ClA 8C1E
111 112
H20 CACl
- - ---------- ----- --------- -- ---- -- - -- ------ ----- ------- -- ----- --- - -- - --- ----- - --... --- - -- - - -- - -- ---------- -- ------ - -- ----
000-001 TP 0 C T' T. TO 1.~ 8 9.1 TR 6.9 6.7
001-002 TR 0 D TR TR TR 1.~ 8 11.8 TO 7.0 6.~
002-005 TR 0 0 TR TR TR 1.5 ~ 8.3 T' 6.8 6.4
005-010 TR 0 0 TR T' TP 1.55 1.68 .028 18.8 9.6 .15 Tp 6.9 6.3
010-019 TR 0 0 TR TP TR 1.~9 1.67 .040 20.5 10.3 .16 TR 6.8 6.2
Ol9-03l 0 0 0 0 a a 12.3 TR 7.6 1.1
031-050 0 0 0 a 0 a 10.3 16 8.3 1.8
050-100 0 0 0 a 0 a 1.5~ 1.61 .015 18.~ 9.2 .l~ 15 8. B 8.2
100-152 TO 0 0 TO TO TO 1.~5 1.50 .012 15.0 5. ~ .1~ 13 8.9 B.2
000-005 1.~1 1.52 .025 21.0
- -- -- --- --------------- - ----- ------- - ---------- ---- -- - ----- -- ------ ---- -- --- - - - --- -- - ---- -- -- ----------- ---- ---------
OEPTH 'ORGANIC MA fTO I IRON PHOS 1- -'=XTRACTA8lE 8Ases 58~A- -I ACT V Al (CAT FXCHI RATIO RAT 10 CA (BASE SAT I
6A1 A 6BlA C/N 6C28 ~N2E 6020 6P28 6028 6HlA 6Glr: 5UA 5A6' 8DI 8D3 5Fl 50 5ci
QFGN NITG eXT TOTl CA >«; NA K SUM 8ACl KCl EXT8 ~HAC NHAC CA SAT eXT8 NHAC
CARB FE eXT8 TEA J:XT ACTV TO TO NHAC ACT V
C. PCT PCT PCT PCT (- -Meo I loa G- - - - - I CLAY MG PCT PCT PCT
-- --- --------------------- - -- ----- ---- -------- -- - --- ----- -- --- ----------------------- - - - -------- ---------------- ----
000-001 2.99 .235 13 9.8 5.1 TR 1.6 16.5 2.~ 18.9 1~.3 .62 1.9 69 81 115
OD1-002 1.62 .1~0 12 B.5 ~. 1 .0 1.1 H.3 2.3 16.6 1~.1 .51 1.8 60 86 101
002- 005 1.38 .121 11 8.9 5.0 .0 1.1 15.0 3.3 18.3 1~.8 .44 1.8 60 82 101
005-01 a 1.01 .098 10 9.3 5.0 .0 1.1 15.~ 2.3 17.1 16.2 .~2 1.9 51 87 95
010-019 .15 .077 10 10.1 6.0 .0 .7 lb.8 2.5 19.3 17.9 .~6 1.7 56 8T 9~
019-031 .79 .085 9 8.7 TR .6 19.3 .59
031-050 .62 .064 lD 9.2 TR .~ 11.1 .37
050-100 .29 .021 11 22.9 .3 .~ 10.1 .~1
100-152 .1~ .018 8 10.9 1.0 .2 6.2 .~3
OO~005
---- ----- ---- -- ------ --- - ------- - - - - ----- ----- --- - ------- --- ------------ ----------- --- -- ------------ -- - -----------
Q!EPTt-t I SATlJAATED PASTEl ~A NA SALT GVP (- - - SA TU' ATI ON exTRACT 8Al- - - I ATTER8eRG
8<1 8CIB SA 502 5E B05 6FlA 8AlA 6N18 6018 6Pl8 6018 61lA 6JlA 6klC 611C 6M1C ~Fl 4F2
RES.T PH H20 ESP SAP TOTL EC CA MG NA K C03 HC03 Cl SD4 ~03 lOID PlST
OHM- SOlU "MHOSI lMI T INDX
C. CM PCT PCT PPM PCT CM 1 - - - - - - Meo I 1I TE' - - - I PCT
-----------------------------------------------------------------------------------------------------------------------
000-001
001-002
002-005
OD5-010
010-019
019-031
031-050
050-100 3~DO
100-152 1500
000-005
6.6 ~9.6
890
2.23 12.9 11.9 .2 2.9 .0 21.1 1.1 1.~ .0
.20C
.10C
.10C
.I DC 32 15 0
.20C
.20C
.~8 .4 2.8 2.1 .1 ., 3.7 .1 .5 .2
2.~5 1.1 10.2 16.0 .2 .0 1.9 .9 2~.S .0 22
8.. 37.3
8.5 31.8
130
56D
-- --- ------- -- --- ----- ---- -- -- -- --- -------------- ------------------------------------ ---- -- ------ - -------- -------- ----
1 AI
1 BI
ICI
101
ClOO OF All. A12. AND A13 FOR BULK D~NSITY AND -.otST"" RETn04TJON.
ESTIMATE
1:2 SOil ~ATfP "ATIO.
8Y SOIl ~ECHANTCS lA80PATORV. USDA. ltNCCLN. NE.
146
-------
A 11,
A 12-'-
A13-
A14-
821t
822t
823
83
C1
Fig. A-4.
Photograph of Ethridge-4 80il profile.
147
-------
Table A-9.
nil !of'If':
Pedon description of 1928-5 soil.
St.,-, !'''Pl' "'1,.: 0 .1] S
HC".:'''': " I/~t ',I II'. iii. ./'', ~1(1 ] 11"- "Hr, I '1 'H OF (OlB-.'. .T.
CL'5\1f"ICtI II "':
."01" \rflU
S" t "0. ~ " !I
no" : ,
.,. ,~...' 0 (l1t.f!
srlL rr.r!l.,q"o'
1"'(' ''''l':
"1 c.,I'" 1',"':
'f..r,IIUI":
''''5IC(,'A.... :
,(,rUTh"
"'('" -'11"''1:
"C'110"
. 11
. II
. ],
( ..
,q.Jttrs:
li1:J'I": ~h lit."'.'!.
{l"! ~. . l '''l' lUll.
A"""I,,: ~, "Il r.lt t \ F
'''!I'UU: 1'1 C.UtS ,
'" P 11\ ~ r . .
'I, ~..
.'"''
HfU'IOhl IOHi Hit.! .0111" ,"'UDI ."'U51
lUlU 'lUor as..,,"
SU"'!!'; ,. O{(,lIttS rill""': '" OU,UfS f
5U,,.(8: ""tUB f Ifltln.: OUi'fn'
IIC""': IU(,U\1 "1101 frdj "Uti TULt
cnt.UOL SHfirt. lIlIlT~ .- U"f'1 D.~ ,. lOMUI iCe '"
L."ur.' (l-SS: sn.t"MU ,."ssnn' runlo
HOtl'JrI(H: cun a
.rll!l' ~~ HillY Ull""O"
.~." 551. ~ "I) 10..1' 5 ."r, 51'RUIS
\\1''''l' ""I1~t'llJ u"CCh~NH"I[ "..tf/'L StDIltfU5
lHl~I'r"~ S'''''}\''''''' "'I' c..LtU'I1...5 !dlI51""i.
It.-crlU Of5ro:!Pl1n"
1 (", ~ t. C I"'.)
t"tj'j \: ,. ~/)) lllL~Hlr . LC'" "'''''' snL ; P.O"~ (Ion "'I) C.U5~fU
-"1'1 ; ~~n flU Pl'" 5taUC'Ullf "IU..c. 10 .fa. '1"(
'~~""IU . 5UfT ,flU fJU'Lf ,~(J~5TJ~.' . hOhPlISUC I
f'''' IoOC1S I"PlJU(~O"" ..'III(" i"'" JIN( l"'fCLiL" '01(5
"nfl' If" IVfH"II' U.Cl) '''111 1 "'I..nu'l:. . ,,"(LilATrl~ H..aLlN( ,". '.6
I t' ~ ( .. ,... ,.. r I. "LV f ) I ,.. j; 1 " a., ! r ')" ( ~ II ,
.. ~II. f t - 1:". )
'~r". ,!.H "/)1 ('L5"'.' . lO"" fT"'. S"..r . "n.", (10" ")) CI\l5"tO
-'.1'1 . .ru , I Jot 'lIt' 51i1UCTUI' .uU"', Te "f" 'I""
I.a"'IIU : 5011 . vrll' fl"'l{ ,~o"HIC" ,IIOh'LaUIr. ;
fIt,' 1>1,111) IHI LIt"'''' ~(J'IlO" ; ""'" F'''I: I.'f(iLl" 'OilS
',1, dill' qH'''I~rH' UI.II (O''''Lrus i -(L(.'1'Il' "ll'lillf ,... 1.2
,.", "'"I'."l "llh) i ,,~" '''II'' "CU"()LI,
~ '., ( 1. t H..)
.rr'.' (1<.". \/)) C'Uto'L ; U"'" FUf 'SUt. ; 8'0"'" CUffI. ,/!) CRU5HfD
.nrq ; wi" ~H" 'll" !1'U(.TUlr '''TIM. HI II'U 'INf
(Ii "'ULU 1 ~1,'1 ,YfPf ""Hf ,hnfi'SlI(II' ,IiIIOh'L'511( I
.,"-, I."" "lIl1S '".UJ{,..t:L1 tor:'IHH . 'I'" "fif ...HUl" '(I'f'S
"11 '~Lf!l' ~fH'''fSrHI (I'U) e.....,u..."U\ i ,r,ClfPITll' IlI"lUIf ,..- &." I
."~W' 1 . .f' ,.. fnL"r .",
~ - J, C... ( l. "". ,
l'"...r "h~"nH f,~" ~;.q "1) CIU\ltfC . F"'. 'Hr, Lca. , lltoH' OLI'~ '10..
\!.'" ~':J C'U\"U; "11',1 ; ..nCle.1f .(£'U' H11' ~"'U(TUI( I ~(Jf1
'f'.' '~ILld ,"'£"HIl" ,,,r.'ll'SlI( : "., 'Ililf '(01S
'1!",u(.tof'u1 "'I filII . ....~ fl'" IJ8J{,Ull~ (t(H! ,
""",UTH' ftHtVI~lfl'" ,"(l' (0"""'Uf'lUS . ~H~"tL' "l'-UHf 'to. ".1
,~)I"'It,..rl ~lllf) ; ~J'~U'I 1iI~'" "nIJlilrUI,
J . J, c... f ". II I...)
I H.., 1,'1f (1.':11' un (8"\"'l ; '1"1 UH. u:." ; (,.nHH SItC". 1.1.5' ~/1J
(PV'",,, '('11,>1 i 1111 flhE "("I""" \fIIUMt ..,("", (T.,,, "f) C.'U5HfD
""'tl'\ ; ,., "I"'" :.Ll{.lflL' ..,I... II'" ~I""U' L(.I" ''It "'(UI" (10" 6/n
'JU' P Ii I'f"ns lO - c' ,..It') I 'I]OtkIH 'Er1U" 'll" ~UUC'U,t
.ll""l' ~~II[ ,\'~' FIIII"U . "O"'!:iTICI' ,.CIiI""S'IC I 'I""
""I "('II, unitt. "HOlt. Cn"')H flhF 1.lIfCULU 'O,,~ ;
vr"l,','l' rffl~vISLf"1 C"U) C.O"U",u(,U\ ; SUDIIICL,llIUIH' '1".I.t
('~L.'''''I'l I1.~U') : (U... 10.." tnu"l,a~'
n' - ':I' ('. ( II - ltJ .II.J
I"..t (,"II L'.H 111) (1.'\HfO ; Fhl \r"'e' U;U I r.IIUUH "'.I.IW" (2." 'ill)
t."J'''''l "t'I~' I "'Co ,,~I(f'" 'It" t-U:C II,J 51"0. LC'" 11'0"" (Ion "J)
('U'.'IlL ft~"'''~ '1'" . C~ T"'C') ; "5Hn . SIIG"'L' H.'O ,
y.P, '-II'U . ,,"Ch1111''''.
148
-------
Table A-lD.
Laboratory analyses of 1928-5 soil.
sc:q I': S -
-SP'Jll MAHRIAl
'J. s. DEPAPTM~'T DF AGRICUl TURE
SOIL CONSERVATION SERVICE, foITSt
.ATIDNAl SDll SUPVEY lABDRATDRY
l I NCOLN, NE BFI ASK A
S1Il ClASSIFICATIGN-
SDIL NO -
- S76"T-D87-5
COU"ITY -
F os FBUD
~FNeRAL METHOOS- - -lA, 1818, 2Al, 28
SAMPLE "105. 16P05bS-7bP0571
-- --- - --- ---- - --- -- ------ ---- -- ------ - -- -- ------ ---- ---- - ---- - --- -- - ------ -- - --- - - -- - -- -- -- -- - -- - - - - -- -- - - - -- - - - - -- --
DEPTH HQR I ZON 1- - - - - - PAPTtCtf ~ lIt: ANAL VSI S, L T 2"", 3A1, 341A. 3AIB - - - - - )RATIC
FINE ( - - SANG - - - 11- - -SIL T- - - -I FAML INTR FINE NON- 801
S".Ni) SILT CLAY CLAY VCOS COR S HE OS FNC: S yFNS CDS! FNSI VF SI TCEXT 11 ClAV C03- 15-
2- .D5- L T l T 2- 1- .5- .25- .ID- .05 .02 .005- SAND .2- TO ClAV BAR
.05 .D02 .002 .0002 1 .5 .25 .10 .05 .02 .002 .002 2-.1 .D2 CLAV TO
CM 1- - - - PCT LT 2HH - - - - - - -I PCT PCT CLAY
- --- - ---- - -- --- -- -- -- - ---- -- ---- ---- -- - ---- ---- -- - -- - --- ------- --- -- ------ - --------- -- -- -- - - --- - - - --- - - -- - -- - - - -- - -- --
DOO-OOI All 76.4 15.1 8.5 .1 2.3 6.7 54.0 13.3 8.6 6.5 63.1 1.02
001-002 A12 19.8 12.6 7.6 TR 1.5 5.3 58.7 14.3 6.1 6.5 65.5 .75
002-005 Al3 80.1 11.9 8.0 .1 .7 4.5 60.0 llt.8 5.3 6.6 65.3 .50
005-010 AC 7B.8 13.Q 7.3 .5 1.0 8.0 59.5 9.8 5.0 8.9 69.0 .4B
010-020 CI 81.3 12.1 6.6 .1 .6 7.7 62.3 10.6 4.6 7.5 70.7 .47
D20-050 C2 7B.7 12.5 8.8 .4 .4 7.2 60.2 10.5 5.D 7.5 68.2 .41
050-100 C3 73.7 14.3 12.0 .4 .5 4.9 52.3 15.6 6.5 7.8 58.1 .41
100-200 C4 73.0 15.7 11.3 .5 .5 5.1 52.8 14.1 7.0 B.7 58.9 .43
100-200 C4 IAI 713.4 17.9 3.7 39.8 14.7 6.5 9.1 B.3 7.6 ID.3 70.1 .57
000-005 18)
- - --- -- --- --- - - - - - - --- - --- ---- -------- - ---- -- -- - - - -- - --- ------- ------ ------ -- - ----- --- -- - --- -- -- - - - - - - - - - -- - --- - - - -- ----
IJEPTH IPARTIClE S!ZE ANALYSIS, HH. 3B. 381, 3B2){ BULl< DENSITV )(- - - -"'ATEP CONTENT- -I C"80NATE 1- -PH - -)
VOL. 1- - - WE I GHT - - - - - - -) 4A 10 4AIH 4DI 4BIC 4B lC 4B2 4CI 6~ 18 3AI A eCIA 8ClF
GT GT 75-20 20-5 5-2 LT 20-2 1/3- OVEN COlF 1/10 1/3- 15- "'D LT LT III 1/2
2 75 .074 PCT BAR DPV BAR BAR BAR CHI 2 .002 H20 CACL
CH PCT PCT 1- PCT L T 75 - - ) l T20 G/CC G/CC PCT PCT RCT CH PCT PC T
- - - -- ----- -- - - ----- -- -- --- -- -- -- ---- - - - ----- ---- - ---- --- -- --- - - -- ---- - -- - - --- -- ------ - -- -- -- -- ---- - -- -- ---- --- -- ---- ----
000-001 TR 0 0 TR TR TR 1.3 C 8.7 6 7.4 7.2
001-D02 TR 0 0 TR TR 1 1.3 C 5.7 7 7.6 7.1
002-005 I 0 0 2 TP 2 1.3 C 4.0 7 7.9 7.3
005-01D 1 0 0 I 1 2 1.46 1.55 .020 13.3 3.5 .14 7 7.9 7.3
010-020 2 0 0 ? 2 4 1.60 1.60 .000 9.2 3. I .10 7 8.2 7.5
020-050 I 0 0 1 1 2 1.5 C 3.6 9 6.4 7.7
050-100 3 2 2 2 1 3 1.39 1.42 .D07 14.u 4.9 .12 11 8.5 7.8
100-200 6 3 4 2 1 3 1.4 C 4.9 11 8.5 7.6
100-200 58 8.B 7.9
000-005 1.28 L. 34 .015 13."
- --- - -- -- --- --- - - -- -- - ---- -- -- -- ------ - -- -- -- -- -- - -- - -- - - - -- -- - -- -- --- -- - - - - -- ------ - - -- -- -- -- ----- ----------- ----- ----
DEPTH laOGANIC ""A TTrp I IRON PH(lS 1- -EXT~ ACTABLE BAS (S 584A- -) ACTY Al (CAT EXCH) ~ATI) PAT 10 CA 1 BASF SAT)
6AIA 6BIA CI~ 6C2B 6N2f 602D 6P2B 602B 6HIA 6Gl': 5A3 A SAbA 801 8D3 5f! 503 5Cl
OPGN NI TG FXT TOTl co HG NA . SUH BACL 'CL EXTB NHAC NHAC CA SAT EXTB NHAC
CARB FE EXTB TEA EXT ACTY TO TO toIHAC ACTV
CH PCT PCT PCT PCT 1- - - - - -MEO I 100 G- - - - 1 CLAY HG PCT RCT PCT
- - -- - - - -- - --- - - - - -- -- -- --- -- -- -- ---- --- ---- ------ - - -- -- -- - -- -- --- ---- ---- -- --- ----- --- -- -- -- -- --- -- -- -- --- ---- -- ------
000-001 4.21 .304 14 4.1 TO 1.2 14.b 1.72
OD 1-002 2.56 .152 17 2.8 TR .5 B.3 1.09
002-005 1.06 .071 15 2.4 .0 .3 6.0 .75
005-010 .59 .044 13 2.9 .0 .3 4.4 .60
010-020 .38 .032 12 3.3 .0 .3 3.7 .56
020-050 .35 .028 13 3.7 .0 .3 4.0 .45
050-100 .45 .036 13 4.4 .0 .5 4.5 .3B
100-200 .49 .03Q 13 4.8 .0 .3 4.7 .42
100-200
000-005
- -- - - ---- -- --- ------- ---- ---- -- --- -- -- ------- - - - -- --- - -- -- - - - ---- -- - -- - - - - - - - - -- - - - - -- - - -- - - - - - - - - -------- --- - -- ---- --
DEPTH ISAT~PAT::D R AS TE 1 NA NA SALT GYP 1- - - SA TIJP A T1 ON EXTRACT 8Al- - - I ATTEA8EPG
8~ 1 BC IB 8A 502 5F BD5 6F 1A 8AIA 6NIB 611R 6P 18 6018 611A 6JiA 6'IC 6LIC 6MIC 4Fl 4F2
RfST PH H20 F SP SA' TOTL EC CA HG NA . C03 HC03 Cl S04 ~03 LOIO PlST
010111(- SOlU ~HHOSI LHI T ,"DX
CH CH PCT PCT PPH PCT CH 1 - M!:Q I LIT EP - - - I PCT
----- - --------- -- --------- ------ --- - --- ---- ---- -- ---- --- -- --------- - -- -- - - - - - -- - - - - - -- - -- - - -- ---- - - -- --- --- -- -- ---- -- --
000-001 6.7 65.7 920 1.77 12.6 5.2 .1 3.9 .0 15.6 1.6 .7 .0
001-002 7.2 4S.0 360 1.10 8.2 2.6 .1 1.5 .0 9.9 .7 .5 .0
002-005 7.6 33.8 160 .6B 5.1 1.3 .0 .8 .0 5. B .4 .3 .0
005-010 7.5 31.9 160 .78 5.7 1.4 .0 .9 .0 3.3 .1 ..3 .0
010-020 7.7 32.3 100 .500 3.4 .9 .0 .7 .0 3.7 .1 .7 .2
020-050 .20D
050-100 7100 B.3 .200 NP
100-200 6500 8.3 .20D
100- 200
000-005
---- ---- --- ----- -- --- - --- -- -- -- --- - -- - ----- --- - -- --- --- -- ----- ------- ------ ------- ---- ---- -- - --- - -------- ---- ---- ---
(AI
I BI
( CI
( D)
WHOLE SOIL, I ~CLl1D 1 NG COUP SE H AG~E~TS, CRUSHED TO PASS 2 MM S I !:VE .
CLOD at: All, A12, AND A13 FOR BULK DENSITY ~ND MQISTUl".r RETENTION.
ESTIMATE
1: 2 SOT l WATF R FA T I o.
149
-------
A11
A12~
A13-
A14-
C1
C2
C3
C4
~
,
Fig. A-5.
Photograph of 1928-5 soil profile.
150
-------
Table A-H.
Sf 11 ~I' I' ...:
"''',n !I'-ru "L.:
UC~'J""I
CLSS\IfUa,p'\:
Sin "'".: ,. t
Slr.' : a
u" ".Ft../lflloll
selL If"I'III&ftJRI
"HI' ""U t
"t(IPITtl'P":
Pl8II'F 'Ii II I":
'''''5IOO-P~':
'1 C II rill ~ " J :
¥(('~U'" HI
"oU.T 'II' w nu
...1,1/,'"
. II
. I.
. I'
, "
. tI
. i.
't! "8IU~~
Pedon description of Riedel-6 soil.
auntL
SH'" In fII
or 1'4, OjJ _I., ..~ ",, Sft( J '11'1, "4tF. 1 "I Sf Of enl5"1', .T.
"~11:.. 11~,jIlIf)IU"f""TS; LOI,., ,..IIFf: (CIU.1dCUS) ,FlI:tC.ID
. StULLt"
,.ru"" .:
C 1 A S~ I
"'.""11 :
1'4NII'LI
'.[P1" :
.'" CII.
"":JloItHLT 01:"10
. IILll',{. II" Hill' UPI""05
" (HSt rF 111(," '(.ft.'
r,1I1 \:,r ~ 'fen J-nIP'S
,lor.toH' w'AUtlArt'
tur~'1 {'IllS c,&..rsy"H
flf'U1Ir,,: 1042 .'HI! -OIiIM H"l£OI lUCUS'
II I f.{H (c.hen, .t';H(U "OITHUn
SU...~8: bII OfGflrfS r "unfIt; 14 DH:;UtS F
5U"",I: OEUfU F 1I1(f.HI, [lEG.FB'
II')"'"' tUr.UH -no: H 'dIU TUiLf
(nft,JIIGl SfClln,. LJII1T5 -- UPHlit OB C" LO"fl: I!!( C.
Cunac.f CLaSSr "ELL &jUlhED
5TOIiIII"'USt cuss iii
n.uu LfVFl
"c. nt 'If( 5 r
n.r.ans ,.
Co.
HH(;II"l .UlIIIILt lOOL rOLL\.''4IH.1I 01 50LlHu(Un
pllOf ILL ur 5[11 PTl.''''
'1. ~ r.. ( t. ("to )
"p(I~" (l.,n 'i/J) (HUH; 51110' Ln... ; 01:. HUO""" BIC"'''' CH.U Cl/4J
'.:1U~IHI) ~USI I ".e.. It "OC(~~H "eCIU" \U""'CULU PLOCIf 5T1U(.IUllf
',S. T ,Hit' f~U'!Lt t hO"'Sf1C" . frtOll'lHTlC 1 (.0".(11 Yt "..,
1('01: oI(CH I~"r)II(,"(JUI 11[')IIUOfrt ; ".,., fl"" UHCUlU IIClf5 ;
-,JU~.lIJL' Hf[IIVtHHl \~(.l) C~hTl"uOU5 I IOCO(llI"U IL'AlPn 'M- f..
~ ~ ,.. 41"'''''l f L Uf ) I'll P J 11,0' ., rv..n "I'
1- ,,(.. ( (- I III.)
"~PI\o'j (l",H ,/J) lPl5to{C I sun, L(lU I Ok. 'EllOIil15H 810"'''' (10n 4114)
'I/IJ<..'L .rlH i .rAl If: IIUOf.'H ~'nll1l1 SlIt"".ULU "VI(I' [lIlY 5T1UCTUI(
~"'I I ".11' 'JoI'"l~ I 11('.<11(.' ,..r"'l'Sflt I to".(. ft PI.'
11 d ,1110'\ 1~"l'jllr,"nu' "J'IIL" 'PU., F I"" IItH.Ullll "CII'5 .
".Hlf~~TtL' qFfIlVfSO"I ""CL) (IJP'''''''''''S . IICU"IIH' 'LIIU"" ,..- II..
~"~ruI1t1,"rL "LUf) ,; 111...(11111' "OU"U40'
.. C.. ( 1 - ~ 1". ')
¥.II)"" (J~'II HJ) (1/IJ!lHfr. ; "~f)' LOAII! ; 0'. TtLLL"'UH "'CIt'" (luU ."'')
L'UI\"ltJ -oBI I tol U Ie .r'C'UH pHIl)' s\.p,..rUllII "\.0(.11 !IIIUC'u'f
',nrl . ".1" ..PUt"L! I H"'HI(1t . ..lJ~"L'511( I (OIl'C. YC '1'"
,".f ../JOT 5 TH'U\I(,I . -"O(lll,,", Il.IU"'f ,..- E.4
t 'P(",''''lIrl ~LU') ; CL'" ~-(r'.. o,nU"'LU'
1'1 - I. ~ ('. t . - ~.) I...)
lll.tI 'lIVI "'0"'" f'1I(,IIClif . ~l P(II('''' 5LltH1L' "1110 lC"" 5ue '''O'''''I5H ''LLO," (ltI'" lit)
I,PU5"'0 Hpn,FICIIHIt.S !l6 - (II ,..", ') ; .'BlYt ; slIc;~n' ""D
~1t".U . "O..SII(I' . "'C'UU!TJC I .."', fJ"'F ,lIfC.ULU 'Olt!
-nn..AI(L' ~rFlo1¥(5Cl"" (JoICl) cr'''''UUt.US . .COFu'H' IlIIll"" ,..- 1.4
C:!WC."""CL PlUf) ; ","01 ,,[.6C~fC ""U',I'U'
.111(, .10... ~'il1b SrJ1l IF-' "'.v C IT "U (-. ~nlL H" 11 116 C' -11j.'J (. Sflve,u.
I 'Jf C.I .tel/un", 15 ,,!\.ftn 1(1 rFCf'llIIf, ,., '"f "'MaT"'" 'I(OIiOel. SI'HlffCl"O.'
U. III U I.II:E (..tot'life "'ro" fllfO'CCI. 10ft Cl "U'lIO" IS 5IlItlU TO . ""LlTHI
C ftl'l1l(l fIfC'" ,.... " B 'tUIfUlf af'l" IIU HOlO IVlIlIflf ",1f'. "O"t:"'..e
'... tt''''''' ol""E1UIf. ''''-''l PLY' I""r",,(''' ':.1¥f5'" '4I-lU.S O.~ '0 t.O fll'''(I'
"'" "'111.
151
-------
Table A-12.
Laboratory analyses
of Riedel-6 soil.
SJ:CtIE S -
-$(" IJ:S NOT (\~SIGNATED
J. S. OEPUT"ENT OF AGRICULTURE
SOIL CONS~RVATION SERVICE. "TSC
NATIONAL SOil SURVEY lA80RATORY
lINCOlN. NE8.ASKA
SOIL ClASSIFICATtON-
SOYL NO
- 57614T-081-6
COU~TY
.OS E8UO
GE-.ERAl 14ETHOCS- - -lA. 1818, 26.l. 28
SAMPLE NOS. 76P0578-76P0587
----- --------- - -- --------- ------ ---------- ---- -- ------------ --- __4____-------------- - -- -------- --------------------
C"
SANO
2-
.05
1- - -
S fLY
.05-
.002
PAPTICLf SIZE
FINfl-- SANO-
CLAY CLAY veas co~s MfDS
IT IT 2- 1- .5-
.002 .0002 I .5 .25
- PCT
ANALYSIS, IT 2M"', 3A1. 341A, 3118 -
- - )(- - -SllT- - - -) FA"l INT'
FNES VFNS COSI FNSI VFSI TEXT II
.25- .10- .05 .02 .005- SANO .2-
.10 .05 .02 .002 .002 2-.1 .02
LT 2MM - - - - - - - - - - - - - - - - - (
- - - - - 100TlO
FINE NON- 801
CLAY C03- 15-
TO CLAY 8AR
CLAY TO
PCT PCT CLAY
DEPTH
HQR t lON
1- - -
-- -- - ---- - -- - - - ---- -- - - - - - -- -- -- -- - - - - - ----- - -- -- --- ----------- --- ---- --------- ------- -- -- -- -------- -- ----.. -------------
01)1)-001 All 7b.'" l~.O 8.0 .8 1.0 1.0 B.2 2Q.8 T.2 7.8 46.6 9 .02
001-002 Al2 16.Q Ilt,1 8.. .0 .7 I.. ..2.,. 31.8 0.0 8.1 .5.1 8 ...
002- 005 Al3 17.8 1".1 8. I .3 .7 I.. H.O 28.4 b.. 7.7 .9.. 8 ..9
005-010 u. 1~. 1 11. J 9.] .' .7 1.3 .1.\ 30.2 8.1 8.9 .3.5 9 ..0
010-025 921 1~.1 15.1 9.8 .3 .3 .8 39.0 H.7 7.7 7.. .0.. 10 ...
025-035 822 11.9 12.9 9.2 .. .. .5 B.2 33.4 5.B 7.1 ...5 9 ..5
035-050 CI 11>.1 15.1 7.0 .1 .1 .. "0.9 35.2 7.5 8.2 .1.5 8 ..0
050-100 C2 85.0 10.5 ..5 .2 .1 .3 50.9 33.5 ..0 5.9 51.5 5 .51
100-116 C3 86.3 9.0 ..7 .0 .1 .9 53.7 31.0 3.3 5.7 H.1 5 ..5
AB 1;.40 15.0 11.0 .2 .. 5.. 55.0 11.8 8.2 7.. 61.6 II .38
- ---- ---- - ---- ---- - --- - - - - - - - --- -- - - -- - ---- - - -- -- - -- - --- - - - - - - - - - --------------------- - ---- -------- ------------ --------
C'
(PARTICLE sIZe ANALYSIS. JlllfII, 36, 381, 382)( 8ULK DENSPY
VOL. (- - - WEIGHT - - - - - - -I ..AID 40AlH 4['1
GT GT 15-2\> 20-5 5-2 l T 20-2 1/3- OVEN I:OlC:
2 15 .07" Pl:l BAI' t'Ry
peT PeT 1- PCT lT 75 - - »lT20 GIeC G/I:e
11- - -
.BIC
1/10
BA.
PCT
-.ATE. CONTENT-
.elc .82 .CI
1/3- 15- .FD
BA. 8AP CMI
peT PCT CM
-) (AP80NATE
6H8 3AIA
l T IT
l .002
PCT PCT
1- -PH - -I
8CIA 8C IE
III 1/2
H20 CACl
I')E PTo(
- ---- -------------- --- - - - ---- -- ---- -- ---- -- --- -- - - - - - -- - - -- --- -- - --- - -- - - -- - -- - - - ---- -- -- -- -- -- --- ---- -----------------
000-001 3 0 0 2 3 5 1.3 A 5.3 8 8.0 7.5
001-002 3 0 0 2 2 . I.. A ..1 8 8.1 T..
002-005 I 0 0 I I 2 1.38 1.40 .005 10.6 ..0 .09 7 8.1 7.5
005-010 TO 0 0 " I 1 1.35 1.37 .005 16.5 ..3 .17 2 8.1 7..
010-025 I 0 0 I 1 2 1.37 1."1 .010 13.5 ..3 .12 1 TR 8.1 7.5
025-035 2 0 0 2 2 . I.. A ..1 12 TO 8.3 7.0
035-050 I n 0 I TP I 1.34 1.<\5 .026 1"'."1 3.5 .15 18 TO 8.. 7.7
050-100 0 0 0 0 0 0 2.3 17 TP 8.6 7.8
100-116 TR 0 0 0 TO TO 1.63 I. .63 .000 2.\ .09 15 TR 8.0 7.8
I 0 0 I I 2 1.5 A ..2 T. TP 8.3 1.0
-------------------- --- - ------ --------..---- ---- ---- ------- -- - - - - --------------- -- --------- -- ------ --------------------
DE PT H (1RGANIC filA TTFR 1 tetON PHOS (- -[ xTP AI: fA 8LE 8ASES 58"'A- -I ",CTY Al ICAT EXCHI RAT tn PAT 10 CA IBASE SAT (
6'IA 6BIA ClN OC28 6N2~ 0020 6P28 0028 6HU OGlE 5AH 5A", 801 803 5FI 5C3 5CI
ORGN NtTG EXT TOll CA MG NA k SU' eACl kCl EXT8 NHAI: Niue CA SAT EXT8 NHAC
CAPB FF E )(T8 TEA FIT ",CTY TO TO NHAC ACTY
C. PCT PCT PC T PCT (- -JIIIf" I 100 G- - - - - - I CLAY MG PCT PCT PCT
- - - - ------- -------- - -- - - - -- -- -- -- ----- - - - -- --- -- - - - - --- - - ----- --- ------------- ---- --- --- -- -- ----- --- -- ----------- ---
000-001 1.08 .095 II 2.3 TR .. 7.2 .8.
001-002 .08 .06B 10 2.. T. .. 0.5 .77
002- 005 .90 .01\ D 2.0 .0 .3 0.. .85
005-010 .9. .08. II 3.. .0 .. 8.3 .89
010-025 .85 .081 10 3.. .0 .. 7.0 .1\
025-035 .55 .05B 9 3.0 .0 .3 5.3 .57
035-050 ..0 .0.1 10 3.0 .0 .2 ..1 .54
050-100 .10 .016 0 3.8 .0 .3 3.1 .0'
100-170 . O. .003 13 3.8 .0 .1 3.. .72
-- - - - ----- --------- - --- - ---- - - --- - - - - --- - ---- -- ---- --- ---- - - - - - - --- - -- - - - - -- - - -- -- --- -- - -- -- -- -- - ------- - ----------
I}EPTH (SUtjPATED PASTE} NA .. S.&l T GYP 1- - - SATU.ATlON E )(TR ACT 8A1- - - - - ( ATTE~8ERG
81: 1 BC lA 8A 502 5E 805 6F lA BAIA ONI8 OJIB 6P18 0018 61U 6JU 6klC OllC O"IC .FI .F2
R~ST PH H20 ESP SAP TOTl EC C. MG NA k CD3 HCD3 Cl SO. N03 lOID PlST
OHM- SOlU "MHOS/ lMiT INOX
C' CM PCT PCT PPM PCT CM I - - - "EO I LITE. - - I PCT
- - - -- ------------------ -- -------- --- ----------- --- ---- ------ - -- - ---- -- --------- - -- -~ -- - -- - - -- - -- - --- ---- - -------- ----
000-001 7.3 30.5 310 1.22 10.9 1.8 .1 .5 .0 10.6 .2 .0 .0
001-002 7.7 31.1 130 .59 5.1 .9 .1 .3 .0 ..6 .2 .. .5
002-005 .208
005- 0 1 0 .208
010-025 .208
025-035 .208
035-050 . 20B
050-100 1900 8.5 .20e
100-116 8100 8.0 .208
----- --- ---- - - --- --- -- - --- -- -- -- ------- -------- -- --- - --- ------ - -- -- -- - --- - -- -- ------- - - -- -- - - -- - -- - - ------- --- ----- ----
1 AI
, 81
FSTH1AfI:
1:2 SOIL WATr;~ J:t.T1O
152
-------
A11,
A12-
A13"""""
A14/
821
822
C1
C2
C3
Fig. A-6.
.,
........,
:~~1I2Q
4
J
,"-A:
~.
e.
.
.'~
..i.....-.
Photograph of Riedel-6 soil profile.
153
-------
Table A-13.
SilL St.,.I:
Sll,( 9 ~, ..l' 110..:
lICUI1,:
(1')(,Hllalll",:
\l1t ""'.; .0 1
SII.": .
." "."'''.111''
UU ".11'111.'
..,f!" 11ft I :
'1''' 'I'll" j, 10'
"..',DII'1':
.. I , ~ I,' t.~ " ,. t :
'I.(tl"I''':
", "' .., .. ~ It '01 ~ I :
..r"uo"
. II
. Ii
. "
. ..
.,-h":
Pedon description of 1928-7 soil.
"01" SPCIU
, "'.'" I'.. lilt 1/4.
C 171'
~rn J II" "1. 1.' s. r' ((!LUlU..'
1'111'11:
l ,\ ~ . :
.....! ~ I :
,.. ,11\"1
" r T '. ~
HI "f."'\
. L All' L('H"
.1. I1'r.,.", r
Pt(,.Jf\ '"
t..
HI.....,n... .l]C .,.,.!
JI"'D I ".atI"
~U'.t'l AI< Of(,UI\ ,
SU'JI": nt'''U\ f
.(j.'''' ,U(.IJSI
("..urn. uc"n, u-." --
C..,uc.r U.'UI SOlll'''tO.I1
.0"'" ''''UD. ."'US'
U'f(U .".
WtllUU H OIC..n ,
"un" DUIUS ,
. '''0' u "nil U'Lt
U",II QH 0 LO.[l1 Ice CII
UCnUYfLt C"hlll
nO.llnu. (,,'51 0
.. '::".
,.,1"
.rl\ 1"1, I'll 'IU.L' U'",'flUS
,11\\',f ~ .r.C to'''' ...u SHflU"
.1 !r.dl' ""'"'11'1' IIIIrfl,,\ULI'UU" ..''''(.1''' \fr'II'."
'H('~I"U5 \U~oST[.f
,Itf IL' Ors(.II'IIOII
I (-. ( ". ~ ,...»
F,"" (I~'" "/1) (II.I\"H J sur' Ln.. . ..U"" (IOU uJ) (IIUStlfll IIlItn
n'.'Iv. ; \1')" . ,..., 'I""'f I "n..\fl(" . flO."lU'U . IUfI'
'I". ..un '..II(,U[""U'tlOIII"" ,,.1IIt ,..., IIIIGU"" 'CIIS .
..')rrlU"", fff(U(SClII' (H(L) ,o..UtoUOUJ . lIoo,.auLt IlU,L(1iII 't!. ..~
(~"I'-1..un bLU() . ..111111" ,nu..o..'
I ~ (II. ( ,,- Ita..)
"All rU:'III. ~~OU fiB (IUSlifO . 51"0' LC,I. . ".0." (IOU u)J'II\n"I.O
..l')lq ; III'" 'u .rO(II'u 'UI. ,....n UI"tY"'f . LOGU . LODSt
.11..\' "" I ",n.'L'\1I( : ,.., fl.' 1100" 1t110U,"0,,' M(!IIlC. .
.':", , t hI. IJUC.UUII 'tilfS I II'not""'" 'ffUUUf'" ("n) ~OfITUUO"S
-O,..,.,IIl' -lIALP" I't- l." l"lot:lon,-q !'lUtl I ".'''".11' 10U.t..,
1. . C... ( I - ~ 11Irj.)
i' -L I ~. 'I~" (I ,'I , I J) llllIJJ"t 0 I s,a.r, l U''I ,"IIICIil.
"I (0 I .'If h. '''(IW.1I (n.l<;t 'L'" SfIo..(flJ;I
n.' ,.,l.lIIll . ,,('1"',11(1' . ",""""111\1(( I ..a""
1""t:tI(,hnlll "0111011 ,,",U,' fl". 1"'.(,UlJI r~1f5
-lIfll~'ln' ffn'YlHHoi (~CL) (L""'UIIU\ 1 '"'N~'''(L'
~".I...I",-PL PLUt) ; 1."~'I.~'t' ,r!j"'[IIII~'
(lUU tin (."SIi'O
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'IhE .COB
I
I.LI.'LI.t ,... 1.4
,- ]J (.. { . - 4 tN.)
nll ,,~~. CI"U III.) (IIIS"IL ; ~."r' ..O.P . A"",,,, (n" 4/') ('U\"'O
"1" .~, ,I! 11 ,,('111 ".1', (f1'.I!-1 'L'" st-", IUlllf I 51)f' .
w .,. ',P,' l' . e,r"\II(" . "("'''l.~tI( I ,I."" f 11111 A(tUS
I"J! ,{It.,,), "lInil" : P'''' .,.( 11I1oI'(,"l.1 'C.f5 I
.~,' ~Ht' rff~'''''''' ("(1,.) (n.., ""(',,, I SU(h!L"U""..' ,,.. I.'
,".' 't"" ,l rllJf) ,,,,,ru'T iii'''' ~ nu..na.,
I, .,,) (II'. ( ,,- ~ P..)
.'.U .'f'I (I.UI 7/1.) {P'I~,.ft . ~.t.r' H'. ; c.."n,. I'n"" (II..~ ~/~)
~~tI5..,n .-"'n' . ,tU ..U"" (lC,1 ")) (H\hft I 'fUO'''SM '111(11" Uti.. "''1
(IUS"'" IIOIU I fU, -rei'" ,.e-Iu", 1\'('1".15" "un.. (Uti .,.) "'''SNID
-o""tS I 1100'111( "H'''.' ('18'51 "a" S"U(tUI' I SC"
.,., flllll'LI: . """'''Icn . ",fJ.'LlSltC I (111110. '0 ...., 'JU
,...rur...oul M(lU,t. I "'" f '.1 III,C,UL" ,CUS I
..nUII'lt ('f(..,t""" ("(I,.) ((":"'I1..unU5 I UIO_U' IUIL.II, ,,.- I..
(l1li;011"'111101. ILUf) I '11"" .." IOU"O'"
100'5
l'. SO (II. ( .. 10.111,)
"'L' "'0"" nou II)) ""5NID I SUO! LO'. I "UO.UN "01111 (IOU '1'4)
(IU5M.n IICIS' . ,au.tO U.SU lIn (IIUS"fD I IIGonN "'0." O'."II"n
(lu5"'0 'CHI I 1(1 'flU'" "(II "..e S"'1I9 LOlli '01 ,.."S" '"0"" CIOU J/l)
(IIU5M.O.O'U 'OUtn 011 CO"'U51IU 11'''''''''0 . t" '''1(.1) I ..5UII. I
UHflll' tllIIIO - fIIIlUti . .0.$1"" - IIO"...UIC . "'II' '.11' loon
'..nUc,H"U' "OUIO- I """ , I..t .II"ULU 'OILU I ft. ""0510"1
. ..r,.f.n )~ ,,, I YIUU.'Lt Utt.nu(", (It".) (o"U.UO&lS I
~'.I( 'C.l' 'L"U.t H- I.' (lI'u'H'un ilL".) ; u.,,,,, IIn, .noIilO'"
~" - I \' 'j (". ~ 1" - ) 9 'III.)
~'l' 1''''". (In. f.I!) (1"'5"fn ; \...r'lr.'. ; H"''''CIilISM IU()III" (It.. SIll!)
.u<."tI -t'JI\' I If ,tlU:"" ~.., .'H ~...n ..[III 'IO~" (1(" 411)') ('UShtC
~(!I.'J "~I -rft.'I'~I!"'C. 11"1 II: III 1\' . ('" U'O) , IInun , SlIC.,.fl' ..",C
DP.,I' . ,,!,"\II(" ,..rJJtII'l'HIC ~ "II fI..r IiCC'S ,,,"",,c,.."U' "0'111..
IIH 1.~'(lL'" ,rlt(!I I ",LUton' (ff(ln"F'" ("(L) (O"IIIIU(lLiS
.HI"'f I' .ll.lIl,..1 ....- I.t ('"IJ"''''''fL "lll') . ""1'l1li.' ~n"'''[ ''''
",It - il J C.. l H - H '''.1
I'. ""II illS I' ,Ita... (,H' ..HI (ilLS I'" I "'-.0' Lnu I ''''lDlUS'' II'~.'" (109' ~")
~1'(Hln -01\1 ~ "S\lw. ; ~Llr,"'L' "'''('1 . fltl.U t .01lS' "I'
',"""lliSUC ~ f.II' IIiIt tllJL'S ,.."NIl,""'" "l'IIIIIL. I ,uln ".,
;I.,I"IIL&II 'II",S I YtrUII'" ~.rrIWf,(f"" (Hl) (OIll""IIOI.IS I
..,.",.r,,,, ""II",lhl 'h- f.. (II.OIl,..'HL nut) 1 h(' 101""10 'null''''
,UT"--''''' SIItoJl5 "".. en"",'. -rlllllt,',' lfyqtr ,t. 1"14. lUG H, 1o, 5UII. 11.
f'. 'u.t r u "0 CI. (",...rlll 'U(.~IS r,O: ,....,111111)'1 ",1[IUL ""'H''' !! Slt''''TL'
"rntf~ I'" "lIult. ROOn, ,IIIOl1l...1." h IIIL:'l.lfn II ,ouns. ,..., SHrUDII' I-
o ",r" ({ tUS "IIiO r'JJtSISTi:h((. I-U !M'\I '''0 5IL15H.' III eJ. 'IIIH'III1T1'" (0
,'It '.III~.:t(;S "ao;O Of t1 HYf.IH ''Ie (' IIIO[ UD IS (II ..It" OCtu. 15 ('('OSIIICUl
flnl'~f\. .-(11)11'111l1li1 ('TII(,II"l.l ,~r.~ FlI"f\ "nl.LUl hi 'fit lJutUOf frc.f 0' '''E
,PIIIL Pl"""'''' -., ~.r..~tJ,' 'M' .~...r. F'Tf"1 ," 'tI( 5'(IL ,,,"H'." rUIIIII' O"C
,11')1. "t'" \U,,(1L'kt ..tt~ 1~k !1'.II(t.... It rUI 'c (CII'I"."" 8' "015tS ".\1
154
-------
Table A-14.
Laboratory analyses of 1928-7 soil.
SOIL CLASSIFICATION-
SrolFS -
- - -5E""S NOT Or;SIGNATEO
u. s. nEPARTMENT OF AGPICLILTURE
SOl L CONSE~VATION SERVICE, MTse
NATIQN"l SOIL SUPVEY lABORATQPV
LINC('lL~, N:8RA$KA
S~IL . NO - - - - - - 57bMT-087-7
COUNTY
POS E8UO
CE"4ERAl -.eTHOOS- - -lA, 1818. 2Al, 28
SAfI4PLE NOS. 16P058B-76P059b
---------------------------------------------------------------------------------------------------------------------
OEPTH HOPI ZON «- ----- PAPTICLE Sill; ANAL YS I S, LT 2"'", 3Al, 34lA, 3AI8 - - - JRATIO
FINE « - - SANO - - - 11- - -SILT- - - -I FAML INTR FINE NON- 801
SAND SILT CLAY CLAY YCOS COR S MF.OS FNE S YFNS COSI FNSI VF 51 TexT !! CLAY C~3- 15-
2- .05- L T L T 2- 1- .5- .25- .10- .05 .02 .005- SiNO .2- TO CLAY BAR
.05 .002 .002 .0002 I .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
C~ (- - - - PCT L T 2MM - - - - - - - - - - -I PC T PC T CLAY
---- ------ ------- --------- ------ --- --- ------ - --- - - - -- --- -- --- - - -- ----- ---- -------- - - ---- -- -- -- --- --- - -- - - --- ----- - - - - - --
000-00 I All 80.5 12.4 7.1 .9 1.4 4.9 57.0 Ib.3 5.3 7. I 6~.2 T .bb
001-002 Al2 82.1 11.5 b.4 .2 .4 3.0 bl.7 lb. B 4.9 6.6 b5.3 b . 52
002-005 Al3 81. T 10.2 B.I .2 .5 3.3 b 1. 2 16.5 4.7 5.5 b5.2 B . 40
ODS-DID AI4 78.3 14.8 b.9 .9 .4 4.0 59.2 13.B 7.1 7.7 64.5 7 .4B
010-020 CI 81.3 12.5 b.2 .2 .4 3.1 62.4 15.2 5.0 7.5 66.1 6 .50
020-050. CZ 80.3 12.3 7.4 .2 .4 3.1 62.9 13.7 5.2 7.1 66.6 7 .41
050-100 C3 75.0 14.9 10.1 .2 .4 4.2 54.8 15.4 b.7 B.2 59.6 10 .41
100-200 C4 66.4 20.4 13.2 .7 .5 3.3 45.8 lb. I 10.4 10.0 50.3 13 .3b
AB
- ---- ----- -- ----- --------- --- --- --- ---- ------ -- -- --- - -- - - --- -- - --- --- - - - - - - - ------- -- - - -- -- -- ----- ---- ---- - -- ------ ----
OEPTH
CM
(PARTICLe: SIZF. ANALYSIS, JIIIM, 38, 381, 38211 8UlK OENSITY
VOL. 1- - - - - - - WEIGHT - - - - - - -) 4AID 4AIH 401
GT GT 75-20 20-5 5-2 L T 20-2 113- OYEN COLE
2 75 .074 PO BAF C'Y
PCT PCT 1- - - PCT LT 75 - - 1 L T20 G/CC Gice
)1- - -
4BlC
1110
BA'
PC T
-WATFFI CONTEf'.4T-
"BIC 482 4C1
1/3- 15- WPD
8AP SAP CJIIII
PCT PCT CM
- - -I
CAPBONA TE
6::18 3AlA
l T l T
2 .002
PCT PCT
1- -PH - -»
BCIA BClf
111 112
H20 CACl
- - - - - - --- ---- - -- - ----- - --- ------ ---- -- ------- -- -- ---- -- ----- -- ------ - ---- ----- - - - - --- -- - --- - - -- - -- - --- - - -- - - - -- - - - - ----
000-001 TR 0 0 TP I I 1.3 A 4.7 8 TR 7.5 7.2
001-002 TP 0 0 TR TR TR 1.4 A 3.3 B T' 7.9 7.3
002-005 TR 0 0 I TR I 1.52 1.54 .005 ..B 3.2 .10 8 TO 7.8 7.3
005-010 TP 0 0 I TP I 1.5 A 3.3 9 TP 8.1 7.4
010-020 I 0 0 TP I I I.bl 1.63 .004 10.ts 3.1 .12 9 TP B.I T.5
OZo-050 TP 0 0 TP I I 1.4 A 3.5 9 TR 8.4 7.7
050-100 TR 0 0 TP TP TP 1.25 1.41 .057 o. I 4.1 .Ob 9 TP 8.5 7.8
100-200 TR 0 0 I TP I 1.2 A 4.8 5 T' 8.4 7.8
TO 0 0 I TO I 1.5 A 5.b TR 8.2 7.7
------------- --------- -- -- -- -- -- ----- - ------- -- -- --- - --- -- ----- ---------- - -- --- - - - --- - -- ------- - - - - - -- - - -- - - - - - - - -- -- --
OEPTH 10PGANIC MATTER 1 IPON PHOS 1- -EXTRACTABLE 8AS ES 5B4A- -I ACTY AL (CAT E XCHt RATIO FlA T1 0 CA C BASE SATI
bAIA bBIA CIN bC2~ bN2E b020 bP2B b02B bHlA bGl1E 5A3 A 5A6A BOI 8D3 SF I 50 5e 1
OPGN NITG EXT Ton CA MG NA K SUM BACl KCL !:XTB NHAC NHAC CA SAT EXTB NH.e.C.
CARB F~ EXTB TEA EXT ACTY TO TO NHAC ACTY
CM PCT PCT PCT PCT 1- - - - - - -MEQ I 100 G- - - 1 (lAY MG PCT PCT PCT
- - ------------------- - - -- - ------ -- ----- ---- - --- -- --- - --- - - ----- --- - -- - -- - - - - -- -- - - - - -- -- - - -- -- -- ---- - ---- ------ - - - -- ----
ODD-DOl 2.01 .167 12 2.8 TR .7 7.7 1.08
001-002 1.10 .069 Ib 2.4 .0 .4 5.7 .B9
002-005 .73 .054 14 2.4 .0 .2 5.3 .65
005-010 .72 .048 IS 2.6 .0 .3 5.3 .17
010-020 .38 .O:il 12 2.7 .0 .2 4.2 .b8
020-050 .24 .024 10 3.8 .0 .2 4.4 .5'
050-100 .15 .Olb 9 b.9 .0 .3 5.3 .52
100-200 .42 .045 9 8.2 TR .3 7.b .58
- - - -- --- -- -- -- -- - ----- - -- - --- - -- ------- ------ - -- - ---------- --- ---- --- -- -- - ------ ---- - -- ---- -- -- - -- - - - - - - -- - -- -- - --- ----
OE PTH ISATURATEO PASHI NA NA SALT GYP (- - - SATURATION EXTFACT 8A1- - - J ATTEPBEFoG
8E I 8CI8 8A 502 5E 805 6FlA SAlA 6NIB bOl8 6P1B bQIB 611A bJIA 6KIC bllC bMIC 4FI 4F2
RES7 PH tl20 ESP SAP TOTL EC CA ~G NA K C03 H(03 CL S04 ~j03 lOIO PlST
OHM- SOLU "4"'HO$1 lJllltT INOX
C~ rM PCT PCT PPM PCT CM « - MEO I llTEP - - - J PCT
- --- - -------------- ------- --- -- -- -- ---------- -- --- ------ -- - -- --- ---- --------- -- -- -- - - -- -- - ------ ------- --- ---- -- --
000- 001 6. B 45.9 1000 2.b7 23." 7.b .1 4.2 .0 29.1 .b .9 .0
001-002 7.b 33.8 220 .90 7.3 1.8 .0 1.0 .0 8.3 .2 .4 .0
002-005 7.7 31.7 130 .58 4.b 1.1 .0 .5 .0 4.8 .2 .2 .0
ODS-OlD 7.e 30.b 100 .48 3.7 .8 .0 .4 .0 3.b .1 .2 .0
010-020 7.7 29.7 200 .95 7.9 L.B .0 .b .0 2.5 .1 b.7 .0
020-050 .20B
050-100 5900 8.3 .20B NP
101)-200 4900 8.0 27.3 90 .41 1.5 3.2 .3 .1 .U 1." 01 ./ .b
---- ---- ----------- -- -- - --- --- ---- ----------- ----- ----- -- --- --- - -- ------- ---- --- -- -- ------ -- --- - -- - ----- --- - -- - - ----
IAI
(81
F5n MATE
1:2 SOIL WATEP uno
155
-------
A 11
A12~
A13-
A 14---
C1
j
C2
I
.
\ '
"
,.. r
C3
L
C4
Fig. A-7.
Photograph of 1928-7 soil profile.
156
-------
Table A-IS.
"h \1 ~II':
\l P V f' ~,' ~ P L r 'I.:
l! ( , I " ,. ~
(r ~ ~ t If II r 1 II ..:
~ 111 "'.; 7.
S,"H:
. . r TO" rt ~ ~ I "p'
~f H If "...~" ~ 1''''1
...,111 't".,:
.. ~ t ( ,.. I 11 1 I ':
PI II" ~ I'll '" :
,.., S I P{,~ f,P.,' :
.. I( anll! ~ III :
wtei' U'H":
"P(~T "r1tQftt:
HURIIO"
. ..
. 11
. IJ
. "
. l.
l Ill'
".
Pedon description of Chinook-8 soil.
1..1!f1.
.11 1/'.
H 11,.e
!1ft'" I Jj II
..~ II". "'.. 114. \1(1 1 n". 1"11, 1.,51 If [1J15"''', "T.
,it."L'" !llIl'lt... (f r.psr~u'!.", I "'un
1 "1I"'t':
IL"o;.:
,\.,(J\I:
>OJ''''''':
-'1'1,:
')1 IInNe,l' ')II."'(
<0' nf(ilf!S f
1)I(,IIff II; f
r..
tl'Vl1ll"; 10)", I'f"k~ "0""" SU'PHO: AU'US'
IIH"!: (nHIYI A\H": SOUTH..fS1
SU"'I~: I.F 0((,"1'( r ..(NUl: 2" D['IU" ,
5u,,,,'II: OHA'U S , III"H~: [If(,lffS'
"'I"n: .urUS1 IhO: 'io!] ..nu UHI
tn"1HJl Sl(lH" L'IIITS n u,rrlf!. a"l) '011 II!.
"lIr,nH' ",Ul1ll1tO
Cil(HI PU" sa"'u\lnfrl'
tlUIClJoil ""1(11, IlOl (CHO'lIUII OR SOlHlU(IIU
PIICflU OfHIIIPTION
'J - 1 (II. ( 0 - 011'1.)
c..'AYI\" ItItO\j" (1"''' 51l) (IIU511(C ; """0' loall ; '4 0It. (j.1"l5tt 811011" (IOU !II)
(,IIU",,!!I 1101\1 ; IC PtRCEl'll S(\fl sun' lOA II' GII"I5" 8tOlltl (lon Ul)
(.IIUSI'I'" kIIOTO'lllrtA5 H - (II nlClC) ; 11100("11 (OUSf .un HIUOUlf
SOf 1 ,¥flU fIlU(lU I "O"')IIC" ,tlON'18511C ; CO" IIIC III flU
"-OOfS UU'OU(,HOUI HO'IIO" ; ...u rtillE IUtGUl.. 'OR£~ I
"o,,-caLCaUDuS (HU) DISCOlllllJilUCUS I II('CEII.I.1fl' HUlI..f ,.... 1.0
(PIIOIIITI1,"ra -tUE) ; "'PIIII,,I, II('U"OAII,
a - 1 CIII. ( o. J Hh)
npow" (I(,YIt "1') (lIl5"E[ ; S"''''' lO'" I ''c. tlt"lSl1 "!lDWI! (IOU JJZ)
1110151 I II. PIII(l~1 H,ft SUrf If'a- V~'" nAPI GU' (IOU JIl) (.IUtO'
JIIU10Yt"as I" . (II ll1lC.l) , IIru "'If CO'1I5E 'un 5111U(1UIIE I
"Of 1 f 'Irq, FIIUtlLf I ~o"""C" . "O"Pl'srI( I (DUO. flM
"OUH ,..1101.1(,1101.11 HC.II(10'" Jill"" F I"'" 1III11(,lIlU POIIF~ . iliA'"
"011'" I "Oi\Ol(U.OII') (I1(L) «ft.Tt"LC.U~ I "CCfUHL' UUUfrlE P"- 1.0
ff\rfHq",II'f'l "lUt) I 111"111"1' PCLI'I[U,
'Jo ,". ( 1 - I. IN.)
'.W!l'.~~ I\IHIII" (I~", H.') (PU"~I( . cs...r'I'-." j ., 0.. ,,In)!H UOII~ (IOU Hl)
'~I':"P "I~I ;!f P:I~'I'1 ~!'rl SHorf lIJU' {D"JS" flIIO.." (nUl ",n
l"l",11! q;,TnYI"~~ l~ - (, ''''0;) ; 'r.r,llIi1l (OiPo;f Plif' UIU('UU
~I.' . 'II'''' ""HI'Ll. 'cntT{.' . ""~Pt'SIIC I (O~-{~ ,,(U
1'1",\ "~C,Lor,II.)U' I'd Ill' . 'H' IIH T~IIf(,\lI'k POlUS I
"I.."(f~llll:' '1(1) {1'''1p.llnl~ , 'OLnnIL' "lIlAlIIilF PH. f.1I
~ ," (""11 ",.. "1 r LlJf , ;.n IIUP 1 . ~ ~, f' uUNfl..'I'
. IL. (-. ( I. - It 11-..)
"",", fl"yr, ..,J) l(oI,\H1, ; ~u.r' 11'- I f./P' -lUll" 'IO'~ ]/!) (llliSWFO
"IIQ . j,. Pf~('" ~1'jT ~'''r1 lr.l" 1'P'(a,~ ~lfJ'1I "l/J) ('liS"'!' IIIC'U.,.",.lS I~
- ~, 1/.Il() ; 'tlfn" l~"'~1 ~l~" S1Pl'(1L'°r f HfI~tll' H"'O
~1"~'lLn . 'IIH1 Ffir/l.l,'n \'..", l',,OIl _~rIU'lllht~ I'.. - (' '''1(') ; 'If"' 11('. CO.II\( ..' 1\11 11 T(
~101ULWI(. '101" liEU (OHH Htt"'.(Ul611 H(1{" ; "..0 f YEll, fll.PlI
t.p""~T'(H . hO"PU!JI( ; {("'u, fU[ .0CIS U.IOUGHCul H(1:110111 I
.....' 1-1'" rllllrr.UI.I.iI '111fS . "'1..(Al"~fOu" (!tI(l) OISCCUI"UCU5
-(l,)fo(UIl' ll'IlIItIE ..~- 11.0 (P"O'H"(l 8ll") : 'PIIl'P1 ~IIOH" prU.f)U'
'Jou - 11Il! CIII. (II. - H T".'
P'lI P-tw, UOH fol]) 'IiUSH't ; H""' In.- i 'l'fLlOIlISH 8'011" (IOU S/.)
(1IIJ""'O "'CIST : Y0' W(n. (f)"H SUJlU,(,Ull'lIIlOCH SUU(TUllf I M<C
'IIrll"RI""LE . ..r"'HI'" . "C"Pl IS" , ; nil' '0 (0l1li0-' fUI! IIOOH
THkUULl1l]UI "1.11110" ; "''''' flH 11III((,Ul'. pOln ,(0111111(. flU
IU~UlU p(..rs I (till. a" SufI ,,,'''Au-Ilk! "HHS (F ll-F I
-OOfIC'lIl" tffUnsU'" (..Ct) (Ot"HOUS I S18.C"Gl' Al....lt~( 't- I.'
(kIlU"''''''II~ BlUr) I G.'OU'l ~"(OH BOU"OIl'
LOu - '''11 C-. (J9 - "9 1ItI.)
Will' r.Ll 1'~1,1i" (u.n Ill) (,PU"H( I S&"" lO." : 'HLOWtSIO PICUI (IDYll. 5/4)
(IIU~IHU "li $' ; VIIH lit" [rIRS~ 'jl1pah,ullII PlC(" SfIU('UU J 10 III (
'IF'" "'UPtf . M;"HI(U ,h("PII5'1( ; Fflil FU,( '00'5
'HI.
157
-------
Table A-l6.
Laboratory analyses of Chinook-8 soil.
SOIL ClASSIFICATtIJN-AF IDle HAPlO~OPOll
COARSE-lOAMY. MIXED
-CHI'400K
SFlltF$ - -
J. S. DEPARTMENT OF AGRICULTURE
SOIL CDNSEPVATION HRVItE, MTSC
NATIONAL SOIL SURVEY LABORATORY
LINCOLN, NEBRASKA
SOIL III') -
- - - 576111T-081-8
COU"ITY
~os ~BUD
r:.Ff.lr:PAl "ETHIJOS- - -1&, 1818, 2'1. 28
SA.PLE NOS. 76P0597-76P0605
-- -- - -- --- --- --- -------- --- --- ----- ----------- ---------- -- - --- --- - ---------------- ---- -- -- --------------------------
C.
SAND
2-
.05
t- - -
SILT
.05-
.002
CLAY
L T
.002
- - - - - PARTICLE SUE
FINEI-- SANO-
CLAY YCOS COOS .EOS
LT 2- 1- .5-
.0002 \ .5 .25
- PCT
ANALYSIS, IT 2"", 3'1, 3AlA, ]&18 - - - -
- - 11- - -SILT- - - -I fAML \Nn
FNES VFNS CDS I FNS I VF SI TEXT"
.25- .\0- .05 .02 .005- SAN~ .2-
.\0 .05 .02 .002 .002 2-.\ .02
L T 2MM - - - - - - - - - - - - - - - - -I
- - IRATIO
FINE NDN- BO\
CLAY C03- \5-
TO CLAY BAR
C LAY TO
PCT PCT CLAY
!)EPTH
HORIZON
t- - -
- - - - - -- - - -- -- - -- ----- ---- -- --- - ---- - - - --- -- --- -- - -- ---- -- -------------------- ----- --- -- -- --------------- ----- -------
001)-001 AI\ 81.7 \2.2 6.\ .1 \.4 7.0 60.3 \2.3 f.l 6.\ 69,,, .12
001-002 Al2 83.8 \0.6 5.6 .7 \.\ 6.5 63.5 \2.0 5.7 4.9 71.8 .B2
002-005 A13 82.5 10.1 6.B .6 .7 5.4 '''.2 1\.6 5.\ 5.6 70.9 .50
005-0\0 Al4 81.9 9.7 8.4 .1 .4 4.9 65.8 \0.7 4.7 5.0 71.2 .44
0\0-025 82\ 80.8 \0.7 8.5 TO .2 5.0 blt.D 1\.6 6.0 4.7 69.2 .47
025-050 822 78.0 9.4 \2.6 .\ .2 4.\ 61.6 12.0 5.9 3.5 66.0 .36
~8j()-1 00 (1(1. 78.7 10." \0.9 .2 .2 3.8 ~O. 2 14.3 5.6 4.8 64.4 .38
100-150 (2(6 bS.'to 19.6 IS.0 T' .4 2. B 'to7." 14.8 \0.\ 9.5 50.6 .37
151)-200 " 7'to.2 14.5 11.3 .1 .2 2.7 50.9 20.3 \0.6 3.9 53.9 .36
- - --- - --- - -- - - - - - - - --- - --- ---- -- --- --- ----- ------ ---- ----- ---- ---------------------- - -- - -- ---------------- ------------
r.
IPAPT1n;: SIZE AN"LY5ICj. "4". 38. 381. 38211 BULK DENSITY
VOL. 1- - - W!:IGHT - - - - - - -) ItAID 'to"lH 1t01
GT GT 7S-20 2(1-5 5-2 l T 2~2 1'~- OVFN COLE
2 75 .074 PCT BAR ~ Y
PCT PCT (- PCT LT 75 - - ) LT20 Glee G/CC
11- - - -.ATER CONTeNT-
4BIt 4BIt 482 4(\
1/\0 1/3- 15- .RO
BAA 8AP BAR (Jill'
PCT PCT 'CT CM
- - -I
CARBONATE
6E \B 3AU
L T 17
2 .002
'CT PCT
1- -PH - -I
8CU 8CIE
11\ 1/2
H20 CACL
Of PTH
- - --- --- - --- - - - -- -- -- - - -- - -- -- -------- ------ - ------- ---- ------ - - -- --- - -- - --- -- ---- -- -- ---- -- -- ------ -- --------- --------
000- 001 0 0 0 0 0 0 4.4 TP 7.4 7.0
ryOl-002 TR 0 0 T' TO TR \.4 6 4.h TO 7.5 6.9
002-005 T' 0 0 7R " TO \.40 \.44 .0\0 \6.5 3.4 .19 TR 7.5 6.9
ODS-OlD T' 0 0 T' TO T. \.48 \.51 .007 23.7 3.7 .30 TR 7.4 6.8
010-025 T' 0 0 7R TP TR \.47 1.«t9 .005 9.5 4.0 .OB TP 7.5 6.B
025-050 7R 0 0 T, 70 TR 1.46 \.50 .009 \0.5 4.5 .09 TR 7.B 7.\
050-100 7R 0 0 TO TO TR \.09 \.53 .009 9.9 4.\ .09 8 B.2 7.5
100-150 TO 0 0 TO T' 10 \.5 A 5.5 13 B.5 7.8
\51)-200 TR 0 0 1 T' \ \.5 A 4.\ \2 8.6 8.0
- - -- - -- -- - ------- ---- -- - - - - - -- -- - -- --- - ---- -- ---- ------- - --- --- ------- -------- - -- - -- -- -- ---- -- -- - -- - - ---- --- ------------
c'"'
IOACANH MATTf~ I
6Al& 681A (,,.
ORGN ~tTG
CARB
PC T PC T
JRO~ PHOS (- -EXTPACTA8LE @&S(S 580\1- -)
6C28 bN2f b020 6P28 b028
FXT TOTL eA JI4G NA K
Ff
PCT PC11---
SUM
E XT8
- -"EQ 1 \00
AC TY AL
6HlA 6Gl'E
BACL KCL
TEA EXT
G- - - -
ICAT EXCH)
513A 516A
EXT8 NHAC
ACTY
-----1
RAT tQ
8C\
NHIC
TO
CL6Y
fliT 10
803
CA
TO
MG
CA 1 BAH SAT I
5F\ 50 5Cl
SAT E X78 NHAt
NHAC ACTY
PCT PCT PCT
F)'CPTH
-- -- ----- - -- ------- -- --- - - -- -- ------ -- - ------ ---- - --- ------- --- ------- ---------------- -- - -- -- ----------- ----------- ----
000-001 2.15 .130 17 2.2 TR .5 \.1 9.0 \.50
01)1-002 1. S9 .092 \7 2.1 .0 .4 .8 7.9 1.«tO
002- 005 \.\2 .075 \5 1.9 .0 .4 .8 7.\ \.00
005-0\0 .68 .061 11 4.9 \.5 .0 .4 6.8 .6 7.4 6.3 .75 3.3 78 92 \08
0\0-025 .52 .052 10 5.3 \.6 .0 .3 7.2 .7 7.9 7.0 .B2 J.3 76 9\ 103
025-050 .42 .038 11 2.\ .0 .4 .6 7.4 .59
0~0-1 00 .24 .026 9 3.2 .0 .2 5.\ .46
\01)-\50 .21 .026 \0 5.\ .0 .\ 5.8 .39
150-200 .15 .0\6 9 6.3 .\ .2 4.9 .43
- - - - - - ---- --- ----------- - ------ ------ --------- -- ------ - ------ --- ------------ -------- ------ -- ------ --------------------
I)i;PTI-I ,S.ATUPAT:D PASTE I NA NA SALT GYP 1- - - - - - SATU"TION EXTRACT 8A\- - - - - - 1 ATT~A8e: fiG
8t: 1 8C\8 U 502 5E 805 6F 1A 8A1A 6N\8 60\B 6P\B 6Q\B 61U 6JU 6KIt 6L1C 6MIt 4F1 4F2
AE Sf PH H20 ESP SOR TOTl EC CA "r, NA K C03 HC03 CL S04 ~03 LQIO PLST
OHM- SOLU "MHOS 1 lMIT INOX
CM C. PCT PCT PPM PCT CM 1 - - - - - - MEQ 1 LITEF - - - - - 1 PCT
- -- - - - - - - - -- - - - - --- --- - - - - -- - - -- -- -- -- ------ - -- -- ------- - ------ ---------- ------------ - ---- -------- - ------- ------------
000-001 7.0 1t1.9 330 \.04 7.2 3.7 .\ \.3 .0 8.8 .7 .6 .0
001-002 .20B
002-005 .20B
1)1)5-010 .\OB
010-025 .\OB
025-050 .\08
(51)-100 b800 8.\ .20B ~P
laO-ISO 6100 B.3 .208
150-200 .208
- - --- ---- ------ -- ----- - -- - ---- -- -- - ---- ---- - - -- - - - - - - --- -- -- - -- --- ---- -------- ------- - -- ---- -- - --- - -- --- ---- ----------
I "I
'6'
1:2 SOIL WATER PATIO
C:ST1f14AT~
158
-------
A11..........
A12-
A13-
A14/
821
822
C1 ca
C2ca
C3
Fig. A-8.
'-
Photograph of Chinook-8 soil profile.
159
-------
Table A-17.
Pedon description of 1928-9 soil.
Sill \"11"
~1,L .,... . -' L' ",.:
l{(,11 ..:
(I .) ~.' " . l' ..:
SJH t.,r.: . ..
~t l Ff :
.1 ~ ,. -, I . fl" ,
SrlL 11 "p(.A1U'\
,It 'I " "'LI:
,~. (. J, J 1"1 ,,,:
"U""" I";
,,,,,)Ir\...t....':
,,'(11"11':
"F'''' .."."t:
"'.""(,
. ..
. "
I'''''' ~HH!I
'I "",
... "". HI I'''. He'
t 11' t
,~. T '''I. """. I P'
H nf' enS1tI', 'I'
\.IIU"'''':
tl ~::..:
~ \""" :
~ . '" I! l :
,,11\":
.11 "'-'11'5
..,HI" u,rl
'" ,,((,lotH \ .
l\,r,lIfl\ f
C'.
fU.,H)fIl.: 1Jll "I HitS
11.11: ,,,,''''f
SUP"(": ", ot 'Iff 5 f
SU"I": ""In 5 f
'(It.H: 'U(.'JH
CO",'OI SIU!U l11i1'TS u
CIU,,,U,f (lISS: 5('111("""
liD"'" S""lfDt '''''UST
""1(11
.U.H': H 0(,IU5 f
.I"UII DIUffS'
. HIOI he wnu "flU
u"Ut 015 (iii lOWEII: Ice c.
fJCfnUt\' CIUUO
nO","[55: CUSS t'
~ I' II
. JIlI.f ," "Ill' II" ."\:5
(,I" '..I) ..t r ,I'" ~
'II {"III' .'"THt"n
'"HI '..,('tiS \'NOUOU
UIlIC"UILSOLIOUf r -'III'-.Il UOIII'.H
u,e CHUUOUS SllBTOht
UHIU OrUI,PTIOh
I Clil. ( C - t' \JIr,.>
ll" t I . ~" ~'" 1 S'1 (,1 a' tl. \. t ,..) t"'. \I'f t
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',lJ~\I'I." II .v"~l'SII( I (()''')''
"oU" ~ "d 'HSICUlU 'n.,~ I
..Iln, Il'JLI",£ 'I;. 1.6 I 'IU1II'"
I te." \u.[ I 0'" Co,n'\101 tUO""
. SCFI I "III' FIU'H .
"1"1 ucn 'HIOUCoHnu'r "'01.,0.. I
-'lOl' (fffIUSU'" (MU) (C"II"\IOU\
"!IUNC..II'
1- ,C". ( \, - I'''.)
I I'"d -~I ~,,~~.. (,.a, l...~' "'l) ('l',,"," . lI)U., SIIilO I IIIfl'
411 "", L (1611!.( pcu, ~tIIU(ll~( .....".(, 10 1I0t'IIU' "ra, fI"t 'll"
',lit 111' "&RH . f'IUlU . "O"UIO' . 1ii0",Pll511C I (O-"J. fU.t
" 1\ 1t'~!,u(,MnuI H,'Tl()" ; PU' n"l IPlI(Col.l'l 'OI'S ,f I.f
1'"" ,I'u(lf'11fl' ff"I'''fHt:.., ""UI cr""l"uru~ I IIBDf"Hl' H.IlH" 'H. f.1
~ II rH' ..1'U"U'~'
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II,..' '.. "tl~H (,11'" ~,.q ,.,1) (IU....fr ; In"., ~,..r . Oil' r,."ISH "110111,,"
"." 414) (IU'"'' "(151 . ..tU .tllUlO Co H"S' ".'" !IRU(IUlf
1 a..I~"', IU lOON""" 'U~, "1..t 'l"" I !.lHM1l' "I,n ,,,rl' fllUPU
, 'I ',I If" . ","",pUH I( . (f".~1 , I'" "LOI!. ,""OUCo"OUI "'['UO" I
. I"r 1."(CUlll rn..n I ,.IJOH'HL' ffrtt"fUfJfI (tIel) (o",rl"'UCI.JS
.l"',',1Q' I.lIAlllit{ .",. '.o! I (t'''l'l wr., t!ru'uu,
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, C("., ~,,,.. I 0'" ~~nnH .iOIll"
yfll' (l'~~t PlU' '5UU('LJlIIf I
,"""""(" . "O.'l'SIH I (01..0111
,.... FIM ,'irCoULU p('fS . 10
; ~f rH"I(C' fFfli,IJS,C(IiiT (I'Cl)
'.' : h"TTP'It' -. OU 111('111 ,
L" 1. (.. t ,,- ,H,'
lll.'" (q, L1.~' 111J C:l:U~'U(, . L~U" SAhli. lIt..1 dIOW"I!.04 (,11" (1."" "I)
','U' ,." .11"1 ; I.," w'" [eUSI Pl'" ~IPUCIUI( I SlIM'fl' HIRC
.' ., .,' ~ ' ( , . ,,( .. ~ 11('" . r.c "rL' Sll { ; ,nppc", f I" I iI ro'!.
1","1 0-,\.,1 "1'~!lf1" ; .rn fl'" IU.tUllfi 'OtiS I 10 Pfll.e...,
'.H"h" '1 ,. . .()f"".iIH' tfflJ'''£S(flilT ('tCl) (f'''Tlft,UOuS
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I' - ' r 'II. ( ~ - o!t, If,.)
.II,~1 lo'" (/.U ",) ('II~"ll ; HI.' srH ; ll('"' .IOIIIIII!.!' r.1I1 'l.!of Ill)
(~"'..II orl..t . LH,H1 \'"If"n.. r,'fl ".'H bId (IUIt.Mfn i {I.II. tR''ISM IIRrVIII
('.'" "'i) (~USHf... .,1\1 I H~ thl " 'HIU' l'iJCII'U"'1 'frOISH !EllO.
L'.'" ~'" CRUSH(U ""'HI', ; 411 Pfllft"'l ,t~, "He. lCI" Slliir llf.HI GII'
Ii ", IIn "u~"1l "l('1 B 0' «("'It,!""r, ".U'IUC" . C. I"IU') I ,.IS5I'I( .
',L""H' I<~~n I '"II' F",flLI I """"',11(" I 1I0"'lISIIC . ff.. f...f
-(I r. 11<~(lUI,H(\U' H'IlLh ; "., ""1 t..ft;.Lilli 'DItS ; HI pIIU..I
'",~,II"t h.ac.'t"'~ )I! (' ,£0 '0(,"1 UlI'5IC"f FllaG"ft,I! I
..r "'("l' u~I"-'~CI"1 (to(l) (f'ft,lUUIU~ ; -COfl'''l' IllI.llIlII' ,..- '.1 I
L l' ,.. .. ~ -. I'ru..';,"
',' . lCK1 C-. (H'" " ,"'.)
lll,II' ..fC i U,III" 51"'1: ; 0.1. Gpun.. "'0111"
f1.H ~/d (IIUS,.(( '(1';1 ; l1[tol t,,, 0.'.1' "II tllUSHIO I
l'~",r '1/IJIo"'5t4 '"t, (I.'" ..,I) ('U~Hrl" 11011',1 ; 10 'fR(IJ"T "fl' "1'0
In.,,, 'H" "IU"" lith ",.) [N""""l PJ{rru 01 CO."ASTJ"G unllllLCf
- (II ftolel) : -.sun ; SlI'''''l' ......n . 'Ifi' FRlUILf I JlO"SYU,"
.,":,rlt'll( . FI.. ""f Neel! ""CUr.MU'MOIIl()" I .,"', FI..r
1~" ,Ill. 'Olf~ I J' ,fllef'" H/It,( ~ll "f r'IC;-f",,,, )1 (It I
""'t
-------
Table A-lB.
Laboratory analyses
of 1928-9
soil.
SOIL CLASSIFICATJON-
SEAlES
- - -SEPIFS NOT DESIG~ATED
u. s. I)EPARTMENT OF AGPICUl TURf
SOIL CONSEPVATION SERVICE, MTse
NATIONAL SOIL $UIWEY lABO~AT('l:ty
l INCOLN, N~BPASI(A
SOIL NO
- 57MH-081-9
COUNTY
POSEBUD
GENFRAL METHODS- - -lA, 1818, 261. 28
SAMPl~ NOS. 76P060b-16P0615
-- -- - ---- - ------ --------- ------- ---- - --------- --- ---- ----- -- --- --- ----- - --- --- - -- - - -- -- - - - - -- - -- - - --- - -- - -- -- - - - - ----
f)EPTH HQR I ZON (- - - ----- - PARTICLE SIZE ANALYSIS, L T 2MM, 3Al, 3 Al A, 3A IB - - - IRATIO
FIN!: 1 - - SAND - - - )1- - -SlLT- - - -) FAMl UHF FINE NON- aOI
SAND SILT CLAY CLAY VCOS CO.S MEOS FNES VFNS C0S I FN$ I VF $1 TEXT II CLAY (OJ- 15-
Z- .05- LT LT 2- 1- .5- .25- .10- .05 .02 .005- S4NO .2- TO Cl AY aA'
.05 .002 .OOZ .0002 I .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
c. 1- - - - PCT LT 2M'" - - - -I PCT PO CLAY
- ---- -------------------- -- --------- ---------- ------- ------------------------------ -- -- -- -- ----- - ----- -- - ------ - - -- --
000-001 411 1a.1 12.4 B. q .2 .0 5.4 57.2 15.3 a.2 4.2 63.'t .42
001-002 Al2 1a. B 11.5 q.1 .1 .4 5.0 51.5 15.a a.o 3.5 63.0 .30
002-005 A13 7a.5 12.6 a. q .2 .3 5.0 5B.l 1't. '3 1. B 4. a 64.2 .3B
005-010 or 1 77.3 13.0 q.7 .2 .0 5.9 54.8 15.8 7.1 5.3 01.5 .34
010-015 AC2 aO.5 11. B 1.7 TR .3 5.1 60.7 1't.4 1.0 4.2 66..1 .39
015-050 CI B 1.0 H.7 7.::\ .2 .4 0.0 61.6 12.8 7.0 4.7 68.2 .4<
05tr100 C2 84.8 0.1 a.5 TR .4 0.7 65.5 12.2 0.4 .3 72.f1 .3a
100-200 C3 B3.3 q.o 1.1 .2 .4 lO.q 00.3 11.5 5. T 3.3 7l.8 .30
100-200 C3 (AI
000-005 1 BI
-------- -- ---- --------- --------- ------ ------ ------------------- ----------------------- - ---- -- ------ -- - --------- -- -- ----
,,~ PT'i
c.
CPARTIClE SUE ANALYSIS. MH, 3B, 3B1. 38211 BULK DENSITY
VOL. C- - - WEIGHT - - - - - - -» 4A1D 4A1H 401
GT GT 75-20 20-') 5-2 L T 20-2 1/3- OVEN COLE
2 75 .074 PCT BAR DPY
POT POT (- PCT L T 15 - - - I L T20 G/C.C G/CC
11- - -
4alC
1/10
aA'
POT
-WATEP (ONTFNT-
'telC 'tB2 4C I
'1/3- 15- W~D
BAR BAR CMI
PCT PCT C~
-I CAR80NAH
bF 18 3ALA
L T l T
2 .002
PC T PC T
(- -PH - -)
8elA 8(IE
III 1/2
H20 (ACL
- ------------- --- ------ --- ---- -- ------------------------------ ---- --------- -- --- - - -- - -- -- - - -- - -- --- ----- -- --- -- -- -- -- --
000-001 1 0 0 TP 1 1 1.5 C 3.T
001-002 1 0 0 TR 1 1 1.5 C 3.5
002-005 I 0 TR 1 TR 1 1.5 C 3.4
005-010 I 0 TR 1 TR I 1.51 1.54 .007 12.5 3.3 .14
010-015 1 0 TR 1 1 2 1.02 1.00 .ooa q.a 3.0 .11
015-050 34 0 la 21 1 34 1.0 C 3.1
050-100 5 0 11 TP TR TR 1.0 C 3.2 B.O 7.9
100-200 13 0 la 1 TR 1 1.05 1..71 .012 13.3 2. a .11 a.5 7.a
100-200 TO 0 0 TR TO TR 1.69 1.11 .004 1.0 2.0 . O' a.5 7. T
000-005 1.4q 1.53 .00q 10.4
- - -- ----- -- --- --- --- - - - -- -- -- -- ------ - ----- --- -- - -- -- -- - - --- -- - -- - --- -- - - -- - - - - - - - - - - -- -- -- - - -- - -- - - - - - - -- - - - - - - - - - - - --
DEPTH COAGAN I C HA TTEP ' IRON PHOS 1- -~XTRACTA8LE aASES 584A- -) ACTY AL teAT EX(HI P AT II) RAT In CA I BASt: SA T I
bAl A 6BIA C/N OC2a ON2E 6020 bP2B OQ2B 6HlA bG 1~ 5A3A SA6A aOI 8~3 5F I 5C3 5(1
(JRGN NITG EXT TOn CA MG NA K SUM BACl KCL Enq NHAe ....HA[ (6 SAT E )(18 NHAC
CAlC 8 FE E xTa TEA EXT A( TY TO TO NHAC A(TY
c. PC T PC? PO POT (- - - - - - - -MEO I 100 G- - - - - - ) (lAY "'t~ PO T PO PO
----- ----- ---- ---------------- ------------------- ------- -------------- -------- ------ - - ---- -- --- -- - -- ------ -- ----- - ----
000-001 1.0a .002 17
001-002 .05 .042 15
002- 005 .50 .036 10
005-010 .3a .02a 14
010-015 .25 .019 13
015-050 .13 .Ooq 14
050-100 .13 .012 11 4.0 .0 .1 3.3 ."
100-200 .oa .001 11 3.5 .0 .1 3.0 .42
100-200 3.4 .0 .1 3.5 .45
000-001)
-- -- - --- - - -- -- -------- - -- - -- - - -- --- - - - ------- -- -- --- - --- ------ -- --- - ----- ------ - -- - ----- - -- - - - - - - -- - - - - - - - -- - - - - -- --
c.
I SATURATED
aE 1 aCiB
REST PH
OHM-
CM
PASTE I
aA
H20
NA
502
ESP
NA
5E
SA'
SOlT
~05
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SOLU
.PM
Gyp 1- - -
bFl' 8UA
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OM 1
6NIB 601B
CA MG
SATUPATION EXTPA(f 861- - -
bP18 6018 blIA bJ1A 61(l(
NA I( (03 HC03 Cl
bUC
S04
- - I
MIllC
~jQ 3
ATTEP8EPG
4F1 4F2
L010 PLST
U41T INO)(
I PCT
1EPTH
PCT
PCT
PCT
"EO 1 LlT~R - -
---- ---- - - - - --- ------- --- -- -- -- -- - -- ----- - --- -- - --- --- ------- -------- - -- - -- ------ -- - -- -- - - ---- - ----- -- - - --- --- - ----
000-001 1.4 30.0 210 1.la 10.0 2.0 .1 1.3 .0 10.1 1.1 . q .0
001-002 1.a 2a.9 100 .55 4.2 .q .0 .5 .0 4.2 .4 .4 .2
002-005 7. B 28.q Qo .41 3.0 .Q .0 .4 .0 3.1 .2 .3 .0
005-010 .200
010-015 .200
015- 050 .200
050-100 a200 a.3 .200
100-200 aTOO B.3 .200 NP
100- 200
000-005
- --- -- -- -- -- --- ---- ---- - -- ---- --- -------- ---- -- - -- - ---- - -- --- ----------- ------- - -- - - -- -- -- - - -- - --- -- -- - - - - - - - - - -- --
1 AI
1 B I
(C I
( 01
SANDSTONE FRAGMENTS.
CLO!) OS: All. A12, AND A13 FO~ BULK DENSITY AND MOISTURE RETENTION.
EST!MATE
1:2 SOH WATcR RATIO.
161
-------
C1
C2
C3
Fig. A-9.
....
..
I
; .,
Photograph of 1928-9 soil profile.
162
-------
Table A-19.
Pedon description of 1929-10 soil.
~I Il \t I n ~:
Slow"., :'1 ''''If 10'.:
l(CATIIJ1to1
(l.S~tr J(H 11111:
un "1'.1 .. I"
'lCP': 1
all 'l ",p~ ~ ~ I UII f
SfH H""UIU.f
10'"' 'I'll:
'~[(II'IIt1If"':
PIli" 'PH '" I
,.., ~ rr c... 'P..., I
"Icenlf l"':
"'.('" III",:
,.. w ~ 1<11 .. r1, " 14l :
I'Cllllro,
. "
. "
II r ~ 5111 < :
~'JU sprlU
.1 1/4,
"''' II.. ",. 1/4,
C 11 J I J
"i. f ~ 'I iii. "4 I .. 1 11"
[~I Cf COt Sfll' I .,.
':Iff ""''''''S
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..(. f'I r,t£( s ,
IHr,lH'S f
co.
fll"'lr..: IClI." .tll"~ .OJrtIH ':I',PlfDI AUGUST
11""01 'lAl.. "SPfe"
5u'.'" tU Ilf tIff S f "'IiIU.: ~4 fltr.AU S f
5uII.I" ", (11£ f \ f ...'IIIUO: ['It(,lIff \ f
,(;..H: 11',"1151 1'''0: he IU". lieu
C.OftoUCl !ttTIl'" 111111S -- U"O: C.d (. lOlltl1 1(( (II'
!,.I'UH. (l'S<;: IIHl 01Il1010
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t I. "1I '_"I',... ~P"loIlil ll.~' I,I'J ("""10ft. V'., r IH >,"r, L ,,-
~ ;,,1' I II 'ft 1'111,,,,,, (l.~' . lto) !"'I.o\t'H, -1)1 \1 ; '"LCI ~'If II J,f
',," II( "J'" . SI t (,,10 tl' '" 50! I' . vi ~, f PI)" 1I ,/IIC"'(' 1(""
~ 1 r ,,,,. "l /I~ It ( :. ",. f I- I ".,f,' ( ,.. or IJf..r L' ..0' II 1 '" ; ..o",
I '111)1 a' (,1,,"" " 'U' I' - II \ . (I. ",n" I I . ~ "" , I It ~ " ' I (. Ll ~ ~ , (I' \
. ''oj \~"..~ 11,111' , ~ I r., ""' \ > 1 .. I (IJ' "I" \ TL '~T', "" f f" ,t'" FIt., < >1. (. I
""l'"..~"t' qp~"fSfI" ft'(l) er_II"L~U~ ; ,IiI("'tl' 'l"LI"t ..~- ':Iot
f I.. II '~'.'Il Illlt 1 ; H r II ~'I" 'r L"0 ~'"
Pl'"
" - .. ('. I ,- - P.)
~II,II ":""'1\1' (,kU l/.~" II() (IOI'...H : ,rp' 't". '"",'" L("!I'
_'I,"" "l!¥l '""I)"'" fl.'>' '>1-) ('l''''l '<11',1 ; "L'"11t '{OI PlI'"
,1~:1(. I!I" . \L Itio"l' M~"v . vr..,.." If "P . "r"lH IC.' . "I')""'LISII(
~...,. , IU lI('l'~ ''''~'u(,t1ru, 1-',JJ/"1o : ...., 'I"f lIJ~IJlU. (O""I"u(u\
"(~'\ . "~II!' ~I'" ",..IlUln """", : ~'" S""""0"" fllltll(IiI''!o
}". I l (J" '11'''' \ 't , \ 11'" I , ~ 't -. " T \ ) 1 '.' :'1] 0' II. 5' ~ l' I" f P, f ~lI '"
~'ILll l'''''I''UOU~ i ~I.,,,rl' .t"l'" ......~ ~.t tPQn..'t1,.nL 'IlL') : (ttlP
~ IY' .. l'u"'I1~"
I 1 - ,,~( '. ( 4 - ,,' 1".1
\ fI,~T r,i" fl.'" 7/~) l"'L.,"'L ;: i(I" ; t H~' rt IVf IIQt,.,IiI ".~,
I 0U' ,.11" ." I <., ; - I ,jf 10:' I' "'I ( T 'J" Pl' " ',' ilL ( IU~ t ; '" I.." I
",,,,'1'(.' I \L1f,I'1L' P('HI( ; ,,~'" r 1\' IIl':1S 1"~.lLfIlOVI
~",'.' '1.,< 'ut-IHIII (O"',,"VI1U\ P(P~ ; r(~.f~ "{.fO "'ll"'~"I.II,
"~(~I"'~ ')1'" I f'io S't1~1('l ,~,(,"'''T', :2 (" ,
.1(,'" 11: L" . ~'I P I'f ',e!' I O.U) ( 1""" ("J', ; '1> ~..( l' It"ll", P"-~. w
('~r.'H'HJl '
-------
Table A-20.
Laboratory analyses of 1929-10 soil.
SEitH S
- - - - - -fillNe SPOIL
:..I. s. DEP'''T"~NT OF AGJl:ICUlTURE
SOIL CONSERVATION SERVICE, MTSC
NA TI ONAL SOIL SURVEY L ASORATORY
LINCOLN. NEBRASIt A
SOIL CLASSI~ICATION-
sntL NO - - - - - - 576"T-087-10
COUNTY - -
posesuo
SAMPLE NOS. 16P0616-16P0624
GENERAL "~THOt'S- - -16, 1818, 211. 28
-- -- - -- --- -- - - - -- ---- - - -- - -- -- ----- --- -------- -- - -- ----------- ----------------------- -- -- - -- - -- --------- ------ ------
DE PT H HOR I ZON (- PAPTltLE S Ilf ANAL Y51 5. L T 2M/I4, 311. 3111. )AlS - - IPATIO
FINE ( - - SANO - - - )\- - -SILT- - - -) FA~L I NTR FINf NQN- 801
SANO SilT CLAY CLAY VCOS COP S ME OS FN:S VFNS COSI FNS I VFSI TEXT 11 CLAY C03- 15-
2- .05- L 1 L T 2- 1- .5- .25- .10- .05 .02 .005- SAND .2- TO CLAY SAR
.05 .002 .002 .0002 1 .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
CM 1- - - - PCT l T 2M" - - - - - - - - - -, PCT PCT C.lAY
- --- - - -- - - - - - - --- ----- - ----------------------- ---- ---- ------- ------ --- - --- - - ---- - ---- -- --- - ----- ------ --- - --- --------
000-001 >11 0\2.0 .6.2 11.1 .4 .5 1.1 26.5 12.9 25.3 20.9 ~9.1 12 .98
001-002 Al2 50.1 38.5 10.8 .5 .4 1.4 30.5 11.9 22.3 16.2 32.0 11 .59
002-005 >13 ~6.0 "0.5 13.5 .5 .6 1.2 25.1 18.0 20.2 20.3 28.0 14 .33
0'5-010 C1 5f'.1 29.1 12.1 .3 .5 1.4 35.1 20.2 16.8 13.0 31.9 12 .41
Ol
-------
A11~
A 12-
A13-
C1
C2
C3
C4
,a
~
.
~
.
J
Fig. A-10.
Photograph of 1929-10 soil profile.
165
-------
Table A-21.
SCH \ -I":
SlI'VI' \t""l' Ir,r.:
LCru 11"fJ,:
Cl'- ~ ~ I 'II ' 1! .J.:
!olft "".: I II
5''''':
till 1f""!".I!"'"
\r11 ".""1\'.'
_" I;' 111 I. I :
'I'll'''''''' ,:
""',1'1",,:
.. t ,. III ~ ~ ~ I , :
'1("[<"11":
'If( , 1 ~ PI ..:
"IP 1~" I 'l:
..,8'1"
. ..
, I:
. oj
Pedon description of 1975-11 soil.
nH !l1'(1l!
.. I".
o 1" 11
,," "'. ..'" 11'. 5'U II ".. '4d. , '1 SF CF ([1.511('. "
IIO.TN SAULFO: AUGUST
15'1(1:
.tlltU': 14 Ot(;'fB F
1111"'1'1 DfC,'f( S ,
. 'lint H ""f' UflLf
11""5 -- u"fU cn '"~ LOMUI lOt ('
"Jr- ".toTfl' IIIELL CUllirlfC
HO"'~fBt (LIB.
IUV"ff'lf\: \''t''j --''''5
UHf "H'
SU",IZ 1\11 :::f GHl5 f
SUI"''': r t r II F ~ S r
."..,,,: ~ IP r II' ,
,,,,,,,,nl '«II',,,"
l:'UUAC..E fL~S\:
1""'/': ." ". ~'IiI"S
US~: "'~l'lf"fl
,",1/\" .. '1,(,lItf5 (
....., ~ I : "t (,I'. t S ,
'1.: r,.
, ('.
. 'I~ , .,/ 1 'l' Slllll
I I Y 'I . r U'''I'l.1 ''''l \.of l ~"[ ~
.. ',I I ~ r , \,) ro~.11 f ~ \ II '"
, ~ ~".' S HI/ ''101~S
.11 'l' .',\'''(II''j UlIIl(lJ.S{'lH'hC .'''t.'l ~H:I..t"T~
I.t Lt.. t,' ,"'.'SH.., '''l I"HIt'ftLfC S"'U ''0 Hll!I(Irt~
,.crlll ttS(ltlI'11"1II
I c.. I I.. J 1"_)
"'c' ',"" d ,. ~'" r,lIl~'Hl . 'I~r, lna" . It'" FUIE '101,.,
I-IH II,'" ; ~"f1 ,w,-, '~Url' I IIO"\IIC" I S\.IC.t"l' PlISllC
'- . "I ~LH!. 1~..'ll0 Il" "(.IIt.. ; -I'" fl"" '(SftUL" '0'(5 I
- '"''1:''' I~H""I\ )' (' I ''1(U''(I' l'ff..'Uf'" l"(l~ (/)lrtU"'UC"S
. ",' f' , , 'l' Al n, ~ ..'" - -.! I"" "r,.., . 01'01 I '" t" ~(lU"O I"
. - . 1-. (, 1 P-.)
,'I' '. -, fI,,'~ ~~J) rl~\"'C , ~'''r' l"L. ; I)'. "llOVIS", e'r"", 110" "''')
, ~U' I, L .r!" ;.' '. 'J"( I'llf' ','..I.". Tl:h . S/)FT
,,'., r.. f.'. l' ,. ,'.\11 c., - ~lIr 1<1l' Pl ,), I( i fhl FI'" 1I0[1S
,,.""II""III...",/r,, ; II.. I,' «(.,rlll '1"( '1f!.!Ll.Jlh ,1l.fS Iff"
,\" ,1.'" I. 'l..t.,\ ).' r. . ~rrJ .'Hl' ''''t''\ltS(l'''' [ttCl) (f"n"t,nus
", ',fl' IlI'I.!'" fl" ../ (.... .FII~J ~ n't-IU'.' 'OU"O'"
(-. ( . - I'''.)
"Il' '.[,." 1.1'h II!} r~L}"dl 1 'I...r' l(~' : II. ,fll/)VI\f' 118("111 (10" ",,,)
,-'1\1 I ,"I~' I.l'~~' "lilt' 'IHIJ(II,,'( . !.OfT
'01' If' '-!lPlf . 'I ~ 1',., ,H 1'1<'" PllI!lT f( I F(.. f 'Jot 'OC'S
If" ('.It. "111 .. )"/(11, 1 If '" 1, (l'" ~ f'''~ lit !lltCl.' '0" 5 . 10' II
I"" ., I" "" < ~ A'," f .. , ) 1 f - ,.r r ! . 'If I.' t f ft . \I~ !lC('" (fttL) (C'" T IIICOU\
.~'Ill' "'''11''( ,,~- ~.I. ,... -t1'''1 , '.,IT.'.' 'OUND",
, '". ( , - . 'I'.J
"l ( .\ (I ,,, ",) ((" ,..t I ; ',IH' l(."~ - ; Ul~[..f!lH 810"'" (111'11 ':II,)
"'1'-.,' J .' "1 ; ,",," (""t. ill.a', 'r.U(TU.~ ; 5llr,H'l' "'10
.o1"..l . "",'~lIt"' ,~llrtTl' Pl""~( I q.. fl"'" loen
.... I'., ," !I,L'll" IL,t'l U (r"II'Ur~!I 'Ctts l(~'OIf fl'l
, ul'" j.>r -, ~ .. '.. ',' "I,' 1( ',I ' 'l ( ., .., S ) 1 (' ;
of, r.'I," f".~I:r" \,«I.J ~ ~'J'UI"!I' . .n(.IIIJlTr~, 'lllllM ...- 11_',
~,oM .'!" I . ,;. II I , ~ ',' , I \.. ",r ,. ,
I " l.. ( ,. II !...)
" 'I' '. "- ~ ( . (,. . 1 '1 r" L' I< f l : .", f" II JI' ., 'l' [1I1!lH 8 lOll" II ,;". ~,.. 1
, ~t. ,...11 . n, q . ~... 1'1' I '..ll'''1I.' "un: I "'I,'lf . ""111";11("
.l f r oil' "t' ',1 I': . (C ,., ''''t..'JtH(U1 "('I'"'' ; ~ HI fl"'t
I 'J "." ,-., I I'L'''l'l I'(pr", ; "'1(J onF l' I'''. w' \(t"T IhCl) (.(It., IIIUrou5
"w"fl' 'I."~ll"" r... <.' ",I" ..,,~. , ~~'I!J" "'Y' I\I'IUft(1al,
" - '. r-. ( J1. 1j p'.)
l'{...1 ,. I' ("'111) rLIt'Hr ; LC'. ; tit..' r-1' (""tin CIII"S"H 1I0ISt
- ",'. 'WI ; 'I I'."fl' "'-I" ,'10'/11 II ,"("',11(." I !lLIr.Mtl' 'LISTIC
""p'.Hl' ',1 "I"".) : .:.o.l.ol' ..." t'fll"JllfI'
.'t - IUII.-. to '<,. " I'..,
, '"" I I "f,' '41 .' , 7',) I fit '... ( . 'I'" r' l ~ 1"
l.llj ~ ,.rf .,. I ';, ..,., 1'1 t ; , r , , ,...' -'I'
'~'I.I'~I'( ,,(l"~"'l' ~f(L"t~(''''1 ~Ii(ll
r ,,~ ~." I." ." < II) ; ..' I "r t (.. r ( 'rL" 1'1 \"
; ~ H,'" ".O"'''I$M ,... f1.~' Iii)
r.,,\'(( . "-I)"SIIC" .
(r"1,,~r~\ . ~U':1HL' 'l!FILlllt
.1-["'.."" '_PIIl~ ".~~ rcl~'w:i', "l'lt.' H(.,uUn '''' 1<;7~. lUG III 1'111. UiIL'
- '. ~ ~1 \) (". "'Ll' ~"I ",1'"l " ,,,, H" 0 II"t (J. .'O'ill U IIOIS'
, ('. >I j .".' 1"" f,', . (II 11 '\'1 " - ',"'," II ., TO , I'~ .
166
-------
Table A-22.
Laboratory analyses of 1975-11
soil.
SOIL CLASSlfICATlON-
SOl L NO - - - - - - S76MT-087-11
COUNTY
ROSEBUO
U. S. DEPARTMENT Of AGR ICULTURE
SOIL CONSERVATION SERVICE. MTSC
NATIONAL SOIL SURVEV LABORATORV
LTNCOLN. NEBRASKA
SERIES - -
- - -SERIES NOT OESIGNATED
GENERAL METHODS- - -lA. IBIB. 2Al. 2B
SAMPLE NOS. 76PD625-76P0634
------------- ----------------------------------------- ----------------------- --- -- -- - -- ----- -- ---------- -- - ---- -------
OEPTH HORIZON 1- - - - - - - - PARTICLE SIZE ANALYSIS, LT 2MM, 3'1, 3AIA, 3AIB - - 1 RATI 0
fiNE I - - SAND - - - 11- - -SILT- - - -) fAHL INTR FINE NON- BDI
SANO SILT CLAV CLAV VCOS CORS MEDS fNES VFNS COSI FNSI VFSI TEXT II CLAV C03- 15-
2- .05- LT LT 2- 1- .5- .25- .10- .05 .D2 .005- SAND .2- TO CLAV BAR
.05 .002 .002 .0002 1 .5 .25 .10 .05 .02 .OJ2 .002 2-.1 .02 CLAY TO
CM 1- - - - PCT L T 2MM - - - - ------ - - -I PCT PCT CLAY
----------------------------------------.-------------------------------------------------------------------------------
000-001 All 13.1 76.8 10.1 .1 .2 .5 5.0 7.3 67.9 8.9 5.8 9 .37
001-002 A12 15.7 15.0 9.3 .8 .8 2.6 53.3 18.2 7.3 7.7 57.5 8 .40
002-005 A13 14.6 16.9 8.5 .6 .1 2.9 52.1 18.3 5.5 11.4 56.3 8 .48
005-010 A14 15.9 16.4 1.7 .5 .6 2.6 55.2 11.0 1.5 8.9 58.9 1 .55
010-028 A15 75.1 15.4 8.9 .5 .5 2.7 53.8 18.2 8.5 6.9 51.5 8 .45
028-050 Cl 13.1 19.2 1.1 .2 .6 3.0 53.5 15.8 8.1 10.5 51.3 8 .56
050-080 C2 68.8 22.1 8.5 .2 .5 3.0 46.1 U.O 10.6 12.1 49.8 9 .45
080-100 C3 61.3 33.1 5.6 .2 .6 1.1 29.9 28.9 19.8 13.3 32.4 6 .61
100-200 C4 74.6 19.1 5.1 .1 .6 2.1 50.1 21.1 1.9 11.8 53.5 6 .10
000-005 IAI
------------------------------------------------------------------------------------------------------------------------
OEPTH
CM
(PARTICLE SUE ANALVSIS. MM. 38. 3B1o 38211 BULK OENSITY
VOL. (- - - WEIGHT - - - - - - -I 4AI0 UIH 4DI
GT GT 15-20 20-5 5-2 L T 20-2 1/3- OVEN COLE
2 75 .014 PCT BAR DR V
PCT PCT 1- - - PCT LT 15 - - - 1 LT20 GIGC GIGC
11- - -
4BIC
1/10
BAR
PCT
-WATER CONTENT-
4BIC 4B2 4Cl
1/3- 15- WRD
BAR 8AR CMI
PCT PCT CM
- - -I
CARBONATE
6EIB 3A\A
LT LT
2 .002
PCT PCT
c - - PH - - I
BOA 8CIE
111 1/2
H20 CACL
------------------------------------------------------------------------------------------------------------------------
000-001 9 0 2 10 3 13 1.5 B 3.1 11 I 8.3 1.7
001-002 1 0 2 8 2 11 1.5 B 3.7 11 1 8.3 7.1
002-005 4 0 2 5 2 T 1.5 B 4.1 11 1 8.4 7. B
005-010 4 0 2 4 3 1 1.5 B 4.2 10 1 8.4 1.8
010-028 1 0 0 1 1 2 1.5 8 4.0 ID I 8.4 1.8
02B-050 1 0 0 2 2 4 1.6 B 4.3 12 TR 8.3 1. B
050-080 3 0 0 3 1 4 1.59 1.62 .006 9.1 3.B .09 14 8.3 7.1
OBO-I00 1 0 0 1 TR I 1.76 1.79 .006 14.2 3.4 .19 17 8.0 1.1
100-200 4 0 0 6 1 1 1.6 B 4.0 9 B.I 1.1
000-005 1.41 1.50 .001 11.1
---------- -------------------------- ---------- --------------------------- ------ --- -- --.. - ---- -- -- -- ---- --- - --- --- - --- ---..
OEPTH 10RGANIC MATTER I IRON PHOS 1- -EXTRACTA8LE BASES 58 ItA- -I ACTV AL (tAT EXCH) RAT 10 RAT 10 CA IBASE SAT)
6AlA 68lA GIN 6C2B 6N2E 6020 6P2B 6028 6HlA 6GIE 5A3' 5A6' 8Dl 803 5FI 5C3 5CI
ORGN NIT; EXT Ton CA MG NA K SUM BACL KCL EXTB NHAt NHAC CA SAT EXT8 NHAC
CAR8 FE EXTB TEA EXT ACTV TO TO NHAt ACTV
CM PCT PCT PCT PCT (- - -MEa 1 100 G- - - - - - - I CLAV HG PC T PCT PCT
-------------- -------------------------------------------------------- --- ------ --- -- -- --- - -- -- ---- --- --- -- --- - -- --- - ----
000-001 .46 .036 13 3.2 TR .2 4.2 .42
001-002 .44 .037 12 3.3 TR .2 4.1 .44
002-005 .43 .038 11 3.5 TR .2 4.1 .48
005-010 .50 .039 13 4.0 .0 .2 4.5 .58
010-028 .40 .039 10 3.7 .0 .1 3.8 .43
028-050 .24 .034 1 3. T .0 .1 3.9 .51
050-0BO .18 .021 9 3.1 TR .1 3.5 .41
080-100 .16 .011 15 4.0 TR .1 2.6 .46
100-200 .29 .014 21 4.2 .1 .1 3.5 .61
000-005
-----------------------------------------------------------------------------------------------------------------------
OEPTH ( SA TURATEO PAS TE 1 NA NA SALT GVP 1- - - SATURATION E XTRAC T 8Al- - - - - - I ATTERBERG
BE 1 8CIB 8A 502 5E 805 6FlA 8AU 6N18 6018 6PIB 60lB 6I1A 6JIA 6K lC HIC 6MIC 4F I 4F2
REST PH H20 ESP SAR Ton EC CA MG NA K C03 HC03 CL S04 N03 LOI D PLST
OHM- SOLU MMHOSI LMIT I NOX
CM CM PCT PGT PPM PCT CM I - - - - - - MEa 1 LITER - - 1 PC T
---------------------------------------------------- --------- --------------- --- --- ------ ------ ------ --- - -- -- - - -- --------
000-001 7.7 25.1 120 .64 4.8 1.9 .2 .4 .0 4.5 .2 1.4 .0
001-002 1.8 26.D 100 .56 3.8 1.5 .2 .3 .0 3.5 .1 1.6 .0
002-005 7.9 25.9 90 .55 3.1 1.6 .3 .3 .0 I. B .3 1.8 .6
005-010 .20C
010-02B .20C
028-050 .20C
050-080 1.8 28.2 130 .10 3.6 2.8 .3 .3 .D 1.6 .1 4.9 .1
080-100 2400 1.6 26.J 350 1.6T 12.1 1.9 .5 .5 .0 1.5 .2 IB.1 1.1 20 3 D
100-200 2100 1.7 26.B 310 1.41 B.5 8.6 .5 .4 .0 1.3 .2 16.2 1.1
000-005
---------- ----------------------------------- -------------- -- --- --- -- ---- ------ --- -- -- -- ---- ------ ------- ---- - ------ ----
lA,
IBI
(t)
(01
CLOD OF All.' Al2. AND A13 FOR BULK DENSITV AND MOISTURE RETENT ION.
ESTIMATE
1:2 SOIL WATER RAT! 0
8Y SOIL MECHANICS LABORATORY, USDA, LINCOLN, NE.
167
-------
A 11
A12~
A 13--
A 14 --
A 15
/
C1
(
C2
C3
C4
Fig. A-H.
Photograph of 1975-11 soil profile.
168
-------
Table A-23.
S( h ~,~ It <.:
SI ~...., <. ft "'1I ',-.:
lrCj\1!11'':
Clj\~ <..' I( PiP":
S 1,. 1\ ,~ . : .. I'
Sir",: t
Alf ,. -P ~ '1I'~1
Sf II 11 "H~~ll'~1
\It" ~ 't Il' :
,p, L 1!llltll ,.
'fP,-,''''IlIT':
I't , ~ 'L(," , I' '-'I' :
"1(111,111111':
'I' r t I IT I"':
,,f~ II I .l II . ! 'I :
1',"1/1'
, "
l I)
Pedon description of 1973-12
soil.
I'tH SP( Il'>
',w ~ I ~.
..; 11 "'. "'.. I I "', ~ r ( 1
{ 11l I.'
1 ~ 11". ~ "'.r. '" ":
.., C' 'UHflP, jOt.
"'1)0,":
lit",:
AI,",.\l:
~ .... II j t :
-1'1,.:
"'1 ",II,"It'\
"" r I ~ A T£ l , \, LI' I '"
~ (, rot..,11 II S r
I'f(,WI.\ I
IUY'''r'''': v'<'H "f1tll~
'II\[: c.r"'C,A'I'I
SUit. [II: t.. ~ Ot{.11 t r s r
su,,,, II: nFC~"'~U'
"II\Tt: ~V,U"T
t 'I''''''' PI ~,( TI .... II" t 1 <. .-
'Ht J"tr,1 (I e< ~: .1 II IIP.\lJr\fI,
"OIirl'tI 'j,JIIIPlf01 'lJ(,UH
ISP£( 1; Hj"H
WflrnlQ: }'" NC.RffS f
WTHU': Of(,pHS F
"11110: "0 wU(' '.PH
IJI'''III: on ell Ifill'''' J(( (It
""- -:".
. <1,11 ~ .'i '
<'JLll"", ,'01 ;.olll' "PlUd',
'.. ~l rio"
S 10"I"t S ~: (Lt SS [,
',~ ,~ ,! ~ r, ~ I
1 'J~ P ~
"1/11 H ~ r ,
t",',ll''''
UHr"Sltlf1t1! n "1"[' H St ~ I-r" l'
~.. r l"lf ~ 'If ('f I SOl 6l r II,,') ~ Ill', r, ~ I
'11(,11'
.'L(\" 'If"
PHflU
[I ~O II'! 11"1"
I l.. r ~ - ','". )
l I' ,. ""J l~ 1 \,<11" : l( '" ; 0- ~ t..." ( I )'~ .., J) (QIJSt-'O .01 P
.. \' . II, r f l" , S 1 Hie 't.J~ r ." < , . ¥ 1 ~, f ~ '.I\l F
,t I , "t' 'I 1 ( , , . " t I' " It' "l t \ I ] ( :. ~.. , I I" I II I) 0 , ~
'Ii' 'II""." 'H,vTII~ ; l""-' II~I '..D'lllt~" Pr.I! : ~d' . 'fl" (QUilt'
'll',l1t' '11(.', . ,LI',I-I[' Pl/lST1( r'''1 Don1"
11" I! -., '11 ..r" II r" :' II..'" 1 I'" ! ~ n r lJl~" I (110
"/1\,-" 1 .. ~~ r, . .1." Q, 1I-l' p, ~ 'r' Sf I'" (j rl) {r"'lIltt.Jnl S
"Tl!.I' ",1I4ll"l ~I-- I." (1'1- ",1110) : f"~'I~/~' ,r'U~l/ll"
(It1JSH( HISI
~ ",r S, r.. 1
.. , j .. l .. < I ~. )
!'/lL' ".'J." (I)f~ f,/J) f~LS~'r : let' : I'.~IJ~" (II'~ ~/JI ('lI.....fn '''1''
.;,~, ...lIlu. (,1t'''llltJ Sf~U(Il~1 . HI',,,lL' "~"l . -,~, f'II"lI
.,1jr,><1l' 'Ill.' . 'II', II' PlA~IJ( ; ~~"" tlH II001S
IflDI"JfI-IUI IJOIlIIl'" : ,~~, ""I 1~~'"llU ~rl'l~ : ,~.. 'f"'''~HNl
I-H"""", ',r. . ." '~~It1' f'ql~'StPd (tn) (""IIJlUOll\
.. It ('l' ~" r I I" P" - J.', V'" . I II ~ j ; /I D" I r II III , ~ f't,. r /I II .
... 1 1 ~. ( ) - "!". )
I"ll "..'.' (IJ'" I'J) lDl',"'! ; l(~~ LI(."" rll" ""'1101. (.;.~, ~,~)
(~II~"I . 1'.1 ; ,,'I' ,lfll" ~t<'Ll'. )1~lJ{Hjll' . 'll(-,~1t' ...t.l
~" l 1 . .. I 1(,,,,, l' 'I! ( . , . ~ It .. , 1 ( . r r,. .,,, 11 "' r " , r p., Q CO, S
I~.,,',"(" '''II~ ; ,,,,\"',11,101 .DU.''''', )'(~ :
. ".. L ~ " t' l..'"'' S ( , '( , H {l 1 (I , , " '. r" " ; .!l" 6 I , .. 1 (.., Po< - 1 - ~ (, ~ p, 11 ~ )
'~'L"1 .fY' ~'H~', fI'
Ii - 11. roo. l Jj - ... r,.)
I T ( I.' !. r :. , ( ~ , 1, ') I; l ') "I I ; ~ Il I 1 (L t, t I. : '~l 1, r r ~ 6 , ( . , . I <) C" t. ',.. I t.
.'1'" :.(. "".C", '"~~" ~ll1' (I" l~. tIL" I~t' r~"'") (~'J~l1 < ., 'I . f 1 ,} :' ~ " I'" ; . ,,' 1 .' ' ~. r.. I t ~ I I ," '1"', , T ( , ,
',tlf,'ft' "l8S'1( , J~H" I!I'~"~(><' If II f(."p,!n,,'
"Il I '-, 't. t t 1". P',- 1.' \"" ,n l' I< J : 'I' ~.. r ..to
,1..11-.1,' <'1 'IL~ "f:D (rt~'~H. "l..fl"'~ -'/',-1'" I' 1'11;. IIJ(. U. I~H
.p <.1.' ( I' '>J l'. .~'" ~,r, ~,~! GIll' ,..r - .. '. YIlt, fl'l' pr"" I~
!.. (I \.~. I~.n(t I Ufrl' (.i ~'.1~1l1' .Ll'~ I' 'r1~'IC!L f~t'1l1t15.
. I ~ 1 1 ~ t j ,'f r r. J I L T"" l.'. I- ,I < ! o. "f. " ", 1 f D I 'l .
sell 1 (
trP'P I
.. OJ t ~
169
-------
Table A-24.
Laboratory analyses of 1973-12 soil.
SERIES -
-REvEGETATEO MINE SPOI L
U. S. DEPARTMENT OF AGRICULTURE
SOil CONSERVATION SERVICE, MTSC
NATIONAl SOil SURVEY lAlORATOn
LINCOLN, NE8RASU
SOIL CLASS IF ICATION-
SOil NO -
- ST6MT-08T-12
COUNTY
ROSE8UO
SAMPLE NOS. 76P0635-76P06.5
GENERAL METHODS- - -1&, 1818. 2&1, 28
-------------------------------------------------------------------------------------------------------------...----------
OEPT" "OR IZON 1- - - - - - - - PARTICLE SIZE AHAl YSI S, l T 2M", 3Alt :latA. 3A18 - - - 'RATIO
FINE I - - SANO - - - 11- - -SIlT- - - -, FAMl INTR FINE NON- 801
SAND SILT CLAY CLAY vCOS CORS MEOS FNES VFNS COSI FNSI VFSI TEXT II CLAY C03- 15-
2- .05- lT lT 2- 1- .5- .25- .10- .05 .02 .005- SAND .2- TO CLAY 8U
.05 .002 .002 .0002 I .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
CM 1- - - - PCT lT 2MM - - - - - - - - - - -, PCT PCT CLAY
------------------------------------------------------------------------------------------------------------------------
000-00 I All 56.1 31.9 12.0 1.3 1.1 3.6 36.1 1..0 10.7 21.2 .2.1 12 .81
001-002 AI2 6..6 2... 11.0 .3 .8 2.8 ~).6 17.1 6.0 18.. .7.5 II ..5
002-005 A13 58.8 28.2 13.0 .. .1 2.7 40.8 1..2 6.3 21.9 "".6 13 .38
005-010 A14 62.7 26.4 10.9 .2 .3 2.. .2.5 11.3 7.. 19.0 .5.. II .55
010-050 CI 68.0 23.5 1.5 .2 .9 3.9 .1.2 1..8 5.3 18.2 53.2 9 .56
050-080 C2 78.2 15.0 6.1 .1 .2 1.7 49.8 26.. II.. 3.6 51.8 7 .31
080-100 C3 33.1 1t9.5 11.. .2 .5 1.2 11.2 13.0 11.9 31.6 20.1 17 ...
100-200 C. II.~ 12.5 6.5 .1 .. 3.. 57.6 19.5 5.6 6.9 61.5 1 ..0
000-005 IAI
- ---------------------- - -- ------------------------ --------- ------------ ------ --- -... ---- ------...--- ------------ ----------
CM
(PARTICLE SUE ANALYSIS, ..ft, 18, 381, 112.. IULK DENSny
VOL. 1- - - WEIG"T - - - - - - -I 4610 .AI" 401
GT GT 75-20 20-5 5-2 lT 20-2 113- OVEN COLE
2 75 .014 PCT IAR DRY
PCT PCi' 1- - - PCT LT 75 - - - I lT10 GICC G/CC
11- - -
48IC
1/10
IAR
PCT
-WATER CONTENT-
.8IC 482 .CI
1/3- 15- ..0
IAR 8AR CM I
PCT PCT CM
. - -,
CARIONA TE
6E18 3AU
lT LT
2 .002
PCT PCT
1- -PM - -,
8CU ICIE
III 1/2
"20 CACL
DEPTH
---- --------- --------- - ------------------------------------------------------- --- -- -- --- ----- -- -------------- --------..-
000- 00 I 2 0 2 I I 2 1.3 8 9.7 12 7.6 7.2
001-002 I 0 TR I I 2 1.5 8 ... 13 7.8 7.3
002-005 2 0 0 I 2 3 1.5 8 5.0 13 8.1 1.3
005-010 2 0 TN 2 2 . 1.6 8 6.0 H 8.2 7.6
010-050 10 0 9 3 . 7 1.11 1.75 .007 9.8 ..8 .08 13 TR 1.2 7.1
050-010 6 0 0 . 5 9 1.7 8 2.6 I. 1.6 7.9
080-100 3 0 0 . I 5 1.7 8 7.6 18 TN 1.1 7.8
100-200 2 0 0 2 I 3 1.69 1.11 .00. 1.6 2.6 .10 13 I.. 7.8
000-005 1.50 1.57 .015 15.7
-------------------------------------------------------------------------------------------------------..---------------
OEPT" I ORGAN It MATTU ' IRON PMOS (- -ERTUCU8lE lASES 5846- -, ACTY AL (CAT EXtH' RATIO RATIO CA IIASE SArI
6A lA 6IIA CIN 6C28 6N2E 6020 "28 6028 6H1A 6GIE 563A 5UA 801 803 5FI 5C3 5CI
ORGN NIT' EXT TOTl CA MG NA K SUM IACL KCl UTI MMAC N"AC CA SAT EXT8 N"AC
CU8 FE EXT8 TEA EXT ACTY TO TO N"AC ACTY
CM PC T PCT PCT PCT 1- - - - -MEo I 100 G- - - - - ' CLAY MG PCT PCT PCT
----------...----------------------------......-------------------------...------------------...---------------------------------
000-001 2..2 .166 15 ..1 TN .1 1.1 .68
001-002 .86 .053 16 3.9 TN .. 5.0 ..5
002-005 ..9 .033 15 ..6 TR .3 ..5 .35
005-010 .38 .027 H ..5 TR .3 ... ..0
010-050 .50 .023 22 5.3 TR .1 ..6 .5.
050-010 .09 .OH 6 ..1 TN .1 3.0 ...
010-100 .35 .024 15 7.0 TR .2 ..6 .26
100- 200 .09 .009 10 3.1 TR .1 2.7 .41
000-005
-- --- -...- - - --..- -.. -- -- --- -..- ---- -- ------------- - --- - -- ------------------ --- - ----- --- -- - - -- --...... - - - - - - - - - - - -... -..- - - --- - ------
OEPT" IS ATURATEO PASTE' NA NA SALT GYP 1- - - SATURATION EXTRACT 1A1- - - , A TTER8ERG
8EI 8C18 U 502 5E 105 6FU UU 6NI8 6018 API8 6018 611A 6JU 6KIC 6L1t 6MIC .FI .F2
REST P" H20 ESP SAR TOTL EC CA MG NA . C03 "C03 CL SO. N03 lol D PlST
O"M- SOlU MM"OSI LMIT INOX
CM CM PCT PCT PPM PCT CM I - - - MED I 1I TER - - - , PCT
- ----------- -- ------- ------------ - - - -- - -- -- --- ...-- - ------ -.. --- - ------.... - - - ------ ..-- - - -- - - -... - - -... -- -- - - -... - - -- -- -- ------ -- --
000-00 I 6.7 0417.1 870 2.22 15.8 9.8 .1 3.2 .0 20.. .8 2.2 .0
001-002 6.1 36.1 430 1..2 9.1 1.2 .1 1.7 .0 10.9 .3 1.5 .0
002-005 7.0 3..e 28C 1.01 6.1 ..8 .1 I.. .0 7.0 .2 1.1 .0
005-010 7.. H.I 190 .81 3.9 3.6 .I 1.1 .0 '.6 .2 2.0 .0
010-050 7.5 27.1 230 1.13 5.7 6.8 .3 .. .0 3.2 .2 10.0 .0
050-080 .20C
080-100 1600 7.1 0411.5 530 1.66 7.9 10.3 1.1 .8 ., ..3 .1 19.6 1.5 H'
100-200 3000 1.0 29.1 270 1.31 5.6 1.1 .9 .. .0 .9 .2 12.7 2.1
000-0~5
.. --.. -.. ---- -- --------- -- - ---- -- - - ---- --- -.. - - -- - -- -- -- --... - ----- -- -- ---- - -- - ------ - - - -- -- -- ------ ------- -- -- --- - ---- -- ..--..-
CAI
181
It I
CLOD OF All, A12, aND 11) FOR BULK DENSITY AND MOISTURE RETENTION.
EST IMATE
1:2 SOIL W"TER RATfO
170
-------
A 11
A12~
A13-
A14~
C1
C2
C3
C4
. ."
. -=--:
..
-,
- .
~
~ "
1
Fig. A-12.
Photograph of 1973-12 soil profile.
171
-------
Table A-25.
Pedon description of 1972-13 soil.
Sf IL ~I ~ ,. '):
SL ''ft, ~..., I' lor.:
L"('111'''1
U'\!.HH&T!r,,:
$I" ..r.: I J
"p'r. .
III' fl'" ""1ul.,
Sill h'" """"1
""'" T 11'1' ~
'''' (I,11'1! ,:
"."." II 11.:
'.' ~ I(C.., ,,.,:
'I('f"d,tlt
"Ht ""rq
'&.'11111 ,,'1'.PL:
"('1/' .
. "
. 11
. "
. ,.
.0'''' ~:
I'UL SPrllS
'.'111 :' ~.
..I I '''" Jot ~'''. .. (,
C lJ1 1)
II 1H. '''if I lit '" ~t ('f (OLU".', ~t.
, W'I,:
Ll' ~. :
)1,1. L~' :
,. .pq:
tlf¥l1JC,": ~':H'!o "U"S '0111'" 5U'LfOI .,"un
1'''('1 (O...tl '$'f(U "fST
SU....O: tP DI(,'US J "lUll' 14 Ot'UE!o f
sup".: f)t.(,'HS f "'11"" DfG"U f
.0"'.1 'U(,U51 . '''01 U Wnu ''!If
("'''H'l SI('O" ,Plln .- U"f', 015 'III lOlltll 100 ell
CII.)UCt (LI.U: IIfll o,.r",u'
SfOJllfjtS~1 cuss 0
Sir .U''''''
',,"'''' HCt".G
46 ''I Lllfl S f
"1'(,111115 ,.
r..
" \"".
.''1'11 ~ 'HI' .""10
L rvq 'III "..r"IIIII"l L'l,,'r~
,~ ~ I I P'
(.~.\,I~ .q If,A~~
t:r 11' .tHI'II/It UJiI(OflsrllDUI[ """!VAl SfDIlIlfIrt.B
'. Al( ;.,"t ~ \'''''1\IIJ"r .,,( ('lc.nfOU~ STll5TCU
'.OF III Of 5'" "'lnJj
1 l". ( (. fJ '''''d
(l",fI/ iH) l~l~l'rr i FIP ~~IrI(" l{..a, . ""(1 (10,51 ~/() (.auS~tO
; .,n'WJU FH£ '1'" HIUC.''''''' '11'1."0111(11 IlfefU"
. ~"t' . vrl' FlrHU "nlrt.5tIt.'. "OJil"'I'SIlC ;,
~L(' ~ 11'"01.1'"0''' I'OIoJlr.1it ; fllAlrt.' f 1"( IIUtU" "OatS
(IOU' (n"""")l5 ; "'UltH ,,,- 6.' ('" IIITUI) i "PIT""'I'
, t. r ~
.''1'1
,~.. "'" f 0
.11.,' <1"(
. '..( \ l t ~~ ( r",~
rY'II/.,
I - ,[,.) c.....\~r t ; su.r' l'l£.
(~IJ'~!'.~I,I 1 "',"''flU "[IIJ~ (,iII.~tJl"lt
¥ 1 ~, I,' J "L' . "I' ' "(" . Joll. 'liS T t ( ;
,...,r'jl.,., ul ,'_rln" . .,,,, f1..f Ilufr,Ul"
{ IOU J ( , ~ " "II n l ~ ;. !l ( l' Ill' .tl" r PII- 1. ~ C Pt<
. 1)'1 ~ ,r. ,
I CI. HllO'llISt- "OWIII (I(U 411)
511U(1UII£ I Sf1F1
..."', FlU I[OB
pr"E~ i "nOl' (FFt'¥fS(f'n
.f1fP) i 'I!IIIU" "...,
1 ~ -' (.. ( .. ,!' I".)
P'lI r.11~'" (ltH "~) ('l'~I,ro ; \lhli'ln., ; "llC"IS" ello,," (Ion, ".)
(1'1,' II' -'1'.1 ; .'~',JII~ ; ~n' . ¥'~, '"1tPU . "O"ilIC"
.,.,ll"llt ;, (I"",t. ;I"f ~lr1< "'~liUr,,,nu' ",'I/C" i lO"D~ flllll
L~"',I,t,~ .,un . '[('''IIHlT "FI""fSCEIII1 \"ClJ [O"TUIUOUS ;
.!ll.l' IltHIIo. ,,,- I.f> (Pt- -IH') i '~~I1,-,II, '(UI.D'M,
'-, - .r., l-. ((L - J'J ,...)
lli.I'r r~" (1'J'" 7,;) (IIUSrlfL ; ',H' lr~. ; "l£ ,'e.'"
"r>I"' . I'~ '[~C,hT 5'" :;Hf\' LII'. lrGHT ",,., (1.S!
- \." 'I :r.) ; -'~"lWf I un . "tll'tIIl.fllf
"o"".nl\( ; ftlll t!"l '-I'OTS If'H'l.If.oHOUT "'''11('1''
f1.,. . .((,~II'lIL' tffU"tH.'" (Hll Cc.llln"tJcus
~," .., I,,, ) i .," r T...r, ",,"'.. [;'"
UC" 6/]J (lUSHfC
fl1) CIUStlH -'''05 c.~
. IIIO"'S1ICa' .
I Hilt FU( IU'GUl..
I IUlOL' Il'llUf ,..- '.t
; ~, - . I l (". ( j ~ - J.. 1...)
.. I', "'I '. ~ . , (I,' ~ "ot) (." l:',.11 r
'('I~r ; ir 't'[I~l ~'fT
\/'11 \ r,... - l. T~lC' ,
t,fllo ~I I ~ ~, . Irt.O"'''l n' IC
.."H ~ I" L' r t~, .. orr «(lJ. T (~(')
. ,I 0(' ~ C ,( ~ ~ t I'" L' ~ ,
, ',""" lI'U" ; ,.tr lit"" U..." "]) c.auSHFC
~"t.r, l"'. "II)(I~H IfllO'll ('.'1" "/0 CItUS"fD
; ."',IH ;, inr, f wfll' FI""l' .
: 'till I t",f !lOc.rs It'IIC\J'"DUT "011110 I
((,"HUt.' ;, "HDl' 'll'Utlf ,..- 1.6 (Pt' IIfHI)
\I~I'.."'! S"flllS UI" [lIlS"III'. '0",""111' 'ft'.nO I" 19'1. 'UC; 11. 1'" SOil'
'''.. ~1'1.~ l ~1 '( ('. a1l l",alU'" .~. "ft'IH AIIt 1['5(11. ruTUhl. "1t.flT 01
IITn,,, It"~ qr ~"
-------
Table A-26.
Laboratory analyses of 1972-13 soil.
SOIL CLASSIFICATION-
seA I E S
- - -PEV~GfTAT'::D MINf SPOIL
u. S. OEPAPTMENT OF AGPICULTUfcE
501 l CIJNSEFo.VATtON SfRVICE, 1415C
NATICNAl SJIl SUP\lEY lABOPATOFlV
lINCOL~t NFBoA5KA
SOIL N~
S76MT-087-13
CCUNTY
PQSFB1JD
GENEqAl M!:THQOS- - -lA, 1818. 2Al, 28
SAMPLE NOS. 16P0646-76PD653
- ---- ---- --- ----- ---- -- --- -- -- -- --- -- ------------ --- - --- -- -- --- ------- ------ ------ --- --- ---- -- -- - -- - -- --- -- --- -- -- -- ----
DIEPTH HORIZON (- - - - - - - - PAFTICLE SIZE ANAL V51 S, LT 2MM t 3Al, ,AlA, 3A18 - - - - - ,"A TIC
r: INc ( - - SAND - - - II - - -SILT- - - -) FAMl INT. FINE NCN- 801
SI.~O SilT CLAY CLAY VCOS CO'S MI=DS PolES VFNS cas I FI'.,s I VF 51 TEXT II CLAY C03- 15-
2- .05- L T L T 2- 1- .5- .2S- .10- .05 .02 .005- SANf) .2- TO CLAY R.-
.05 .002 .002 .0002 1 .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
CM 1- - - - PCT LT 2"'''' - - - - - - -) PCT PCT CLAY
- - --- ---- - -- --- - - -- -- ----- ---- -- --- - ----- ------------ --- -- ----- --- -- ------ -- - -------- --- -- -- --- --- - ------- - - --- -- - ----
000-001 '11 61.4 28.\ 10.5 .0 .4 1.1 46.7 13.2 19.4 8.7 48.2 .93
00 \-002 Al2 1q.l 11.1 9.8 .1 .4 1.8 60.1 16. T 5.4 5.7 b2.4 . 3~
002-005 013 80.8 13.1 6.1 .1 .5 1.8 b3.8 14.6 4.[ 9.0 66.2 .62
005-010 '14 Bl.b 11.5 6.9 TR .4 1.9 62.9 16.4 4.2 7.3 65.2 .51
010-050 CI 75.5 16.8 7.7 .3 .5 3.6 58.6 12.5 3.1 13.7 t3.0 .45
050-100 C2 71.2 25.0 3.8 .0 .4 3.4 59.6 7.8 16.7 8.3 b3.4 .55
100-200 C3
000-005 (AI
- --- ------ -- -- --- -- - - --- --- --- ------- -- -- -- - - --- - - - -- - - - -- -- - - --- --- -- - - ---- ------ - - -- -- -- - - -- - - -- -- -- - - - -- - - - - -- --
F)C:PTl-1
CM
(PARTfClf StH 4NALYSlS, MM, 38, 381, 36211 BULK DFNSITY
VOL. (- - - wEIGHT - - - - - - -I 4AlD 4'IH 401
GT GT 75-2020-5 S-2 LT 20-Z 113- OVEN COL'
2 15 .074 PCT B"q OJ/Y
PCT PCT t- - - PCT LT 75 - - I LT2J G/CC G/CC
1(- - -
481C
1/10
8'"
PCT
-WATH CONTENT-
481C 482 4Cl
1/3- 15- WAF)
SAP 8AFt CMI
PCT PCT CM
-I CARB'JNATE
b~18 JAIA
L T L T
2 .002
PC T Pc. T
(--PH--J
8CIA 8CIE
111 1/2
H20 C.AC.l
- --- - -- - - - -- - - -- - ----- - - -- -- -- -- ------ - --- -- - ---- ---- - -- -- ----- --- ---- -- - - ------ --- --- -- -- -- - --- - - - - - - - -- -- ---- - - - - - - ---
000-001 1 0 0 0 2 2 1.2 8 9.8 TP 1.3 6.3
001-002 TO 0 0 TP TP TR \.4 ~ 3.T 3 7.8 7.3
002-005 T' 0 0 TP TR TR 1.4 8 3.8 3 8.9 7.3
no5-010 TR 0 0 TP TP T' 1.5 8 3.5 3 '.1 T.5
010-050 7 0 0 7 4 11 1.5 8 3.5 11 8.4 7.7
050-100 TO 0 0 T. T' T. 1.5 8 2.1 \2 8.5 7. T
100-200 TR 0 0 1 TP 1 1.5 8 2.0 12 8.3 7.6
000-005 1.39 J. .39 .000
- - --- ----- -- -------- - - - - -- -- -- --------- ------ -- -- - --- --- - --- --- -- - --- - - -- - - - - - - -- - - - - - -- ---- - - -- - - - - - --- ---- - --- -- -- ----
DEPTH (OAGANIC MA TTFR 1 I 'ON PHOS (- -EXTPACTAf!LE 8Ases 584A- -I ACTY .\ (CAT EXC"'. f< AT I) PAT to C' (8ASe SAT)
bAI A 681A CIN 6C28 b~2!: 6020 bP28 6028 bHlA 6GlE 5A3A 5A6A 801 803 5<1 5C3 5C\
ORGN N1TG EXT TOTL CA MG N' K SUM BACL KCL ':XT f' NHAC NI-IAC (0 SAT E XT8 NHAC
CARB FE fXT8 TEA ~XT -CTV TO TO NHAC A(TV
C~ PCT PCT per PCT (- - -MEO I 100 G- - - - - - - ) CLAY "G PCT PCT PCT
- --- -------- ----- ----- -- -- -- -- -- -- - - -- ------- -- -- - -- - --- -- ----- --- ------ --- -- - ---- -- -- - ---- -- - - -- - ------------ -- -- ----
000-001 \0.00 .316 32 5.8 T' 1.\ 5.2 24.9 2.3T
001-002 1.72 .078 zz 2.5 TP .5 T.O .Tl
002-005 1.07 .067 16 2.4 TR .4 6.1 1.00
005-010 .54 .053 10 2.3 .0 .3 5.1 .74
010-050 .1 Z .013 9 3.9 .0 .1 3.7 .48
050-100 .05 .006 8 2.9 .0 .1 2.3 .tl
100-200 .07 .005 14 2.9 TO T' 2.2
000-005
- -------- - ----- -- ------ --- ----------------------- --- ---- ----------- -------- -- -------------- - - --- -- - -------- ---- --------
OEPTH C SATURAT~D PASTel NA NA SALT GYP (- - - SA TUfO A Tf ON eXUACT 8Al- - - I ATTHBEFIG
8El 8C 18 8. 502 5E 805 6F 11. 8AIA 6NI8 6J 18 bP 18 bO 18 bItA bJIA 6K IC bL IC bM1C 4Fl 4F2
REST PH H20 ~ SP 5" TOTL EC C. ~G N' K C03 HCCJ3 CL S)4 ~'03 La 10 PLST
OHM- SOLU MMHOS/ U11T I NOX
CM CM PCT PCT PP" PCT CM ( "EO I 11 TEl". - - - - 1 PCT
- - - - - - - - - --- - - - - - -- -- -- -- - -- ------- ---- ---------- - -- - --- -- -- - -- ------ - - - - - - - - - - - -- ------ ---- - - - - - - - - -- - - - -- - ---- ---- ----
000-001 6.7 60.5 1100 2.09 15.0 8.4 .\ 4.0 .0 I B. ~ 1.. 2.0 .0
001-002 T.3 33.9 240 .95 7.0 2.6 .1 1.4 .0 7.2 .9 .7 .0
002-005 7.4 31.5 240 1.01 7.8 2.9 .1 1.1 .0 7.8 1.1 .7 .0
005-010 7.8 31.0 120 .56 3.8 1.1 .0 .5 .0 4.2 .3 .3 .0
010-050 .20C NP
050-100 6100 8.1 .20C
100-200 3100 8.0 28.8 280 1.3~ 6.3 6.0 <.< .> .f . T lb. 7 .0
000-005
-- --- - -------- --- -- -- - ---- -- -- -------------- -- -- ----------- -- -- ---- - -- - -- - -- --- -- -- - - ---- - --- - --- --- ----- -- ---- -- ----
101
(81
! C I
CLOO OF All, A12, AND A13 fO~ BULK DfNSPV AND MOIST'JRE P'=TENTION.
ESTIMATE
1:2 SOIL WAT~P PATII')
173
-------
A 11
A12~
A13-
A14/
C1
C2
C3
,
.
f
Fig. A-l3.
Photograph of 1972-13 soil profile.
174
.' ,
,
-------
Table A-27.
srll !If'1! 5;
'''Iwn Sj."Lf "'0.:
LOCATIO,..
U'SSIFIU1Tf''''1
S" E "0. ~ 0.-'
Ilt"'" I
IU n"tluutf
SOL Tf 'Ptu'uu
"UtA UHf'
PltCl",,'IC"':
'.llIf.flU,"':
''''SIC.''''''"' :
..IC'OflflU. ;
WICifUtJCIilo'
"'t.., ..H."ll
~O.lIO'"
. ..
. "
.,,,.. SI
Pedon description of 1969-14 soil.
u.. $'1!1l 5
a IH ..
,~ 1'''- iii" ."', "''' ""- un 17 TU, '''If. " III' Sf Of tOlStIl', ",.
SU '(IU-"5
"fIIL'LnH
l1li6 I')f.CiREES F
I')tc.ltffS F
C,.
ILEWHI(!JU 0911 ..nfls "OUtI S""LEU IUCiun
1..01 cO"cnl ASPECT' .OI1MWUT
5U""tl' 68 DfG.US f "lUff' H OH'f!S ,
50'''(1' nfC,IUS f "''''11' Df"US II
IIO'-t, .uC.U51 UNOt file Vutl UIU:
COliionOL SECTIC" LI"IT~ -- uppru GH CfI lOVUI Ice u
Ol'lun cuss. "fU OIllU(O
nU.lllfSSt cuss 0
lnu..,' I
(LU~I
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n(Pt!i:
:""., ".
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1"1 SLCI.t
C.USSfS ".0 tOIlU un 5..IIU,,,
"'lIGfitl' IfEUt-HI t U'COI!SOllD,1fC .",UI\ UtilUn
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ll(.111 """, \111" Jill CflUSltfD . FU,f SUOT LOUI : ,.nISH "0'" (10" "1)
c.'uSttfn ."IST . "111 TO (0."0. (NUf ,'O"U,hT suo.., 1.ollN 0."11 ~II)
(AU\"(O "OITL.FS I ,"fIt tlIn. flU 'un STtuCtult . SOFT
'HII' UUHtr. . IIIUSIIU' . UIG..TU'LUTH . un F.., .oon
"'4I"II(.""U' Hnl"ON I linT fn.f JlCUC-ULU 'OafS 1.1.0 "ICE"T
IItaF,) !»fUI"ENU" fPAC;'f'-n, >1 1111 ; IIUDL' fFFI"U(UT (tI(L) (O""UOUS
~lIr.Hl'l' -(II) ..,.. 6.J ('I' '(H5) ; "BlU'" 80UIIO..'
1 - 1 C.. C, C. - 1 IN.)
llC-flT f,IIH \IOTA Jll) "U\l1tO . 5"JrlOT LOU; (,''''15" 8IOtl" (IO'U ",n
(.RUSHFr !I(jIS' . Hili TC COII'O. ((lISf "OIlI'U' \I'O"C; 1110". U."'""I)
(.AUSottU II01TlfS ; YEn "UI 'HE PL"" \T.1~CT....t . SOfT
yon, ('HIIU . "'(IIIHHII' . SllGhn' 'UUIC I -I'" f..' 'OOTS
IH'OU"'"OUT HOIUO. ; IIAU I' ''''I III'HUlU 'ORfS . I'CI .nth'
"UIO ~fOl11f"TIUU ,..c."""Y!. )2 II" 1 PlLOU [fH'YFSU.' (t4[L) COUIIIUCUS
~IlOU AlUlI"-E 'fI- I.) (,to fI' nn ; ,II'IT.'" ~OU"CI"
, - ~ C-. ( 1. , I"'.)
LlCtH' nOll..UIt 'IAT (lOU 61t) (tUS"IO J fl"'f 5"'0' LO'JI . G''''I1" "0..
(JOT... "1) C'uS"fC 'CISI I Fr" f( tC,..tlrl conse "OIlUUT 5,.0'" RIO""
"I.~" "'II) C.uShEO "OTTUS I "tII'IItu n..t 'ltT' snUtTUIf I SOfl
yfll, f. U'U . "'UST 1(1' ,Sl I'hn' '1."\11( I ".., , hi 'OOU
1""OU(ltI)UT 1t0.flU 1 'I'''' FHE Itllf(.ULU IIOIU 1 1 'fICUI
-'1'11 SFO'.'",u, fPH.IIHU )l'" ; JlHOI' (fFltnSU'" ("Cl' COlnIllUC.US
-IlOL' "Lilli"' 'It- I." "," "tH.) I Clf" !If"" !OUltO'"
~. 10 C". ( I.. "HI.)
LTc."' "'0"'-15" C;U' OOTl: 611) ClLSt'rc I SUO' Lt.. 1 c.lnn,. UOII.. (lUt "t)
\"RUS"tL .ll~,' : n" Ie ((.1I,OJi, CCI"H "C'I"u.' STIIO~C; 'UIO"" (1.'" 511)
(RU~"rr) ,0TTLfS : y", IIU" FlU 'LITT UlluttU.f I SOfT
YFII' U:U!U . SUGtoH' S1I(" . SlIG"tl' 'LJHJC 1 .."",
'DOH "'''OUCo'''OUT "OHIO'" : .U' I' HIt l"fCoULU 'OU\ J
"If 0 HOIIlE,,"IT ,U'."U >1"" ,; 'l\.Ol' ffFUYfSUIII' (hCt)
"fllf!llL ,"- '.J ('h '1"'11) 1 ".11'''' II(lUNO'"
fhl
I "'(UT
eOlllYlNUOUS
I C. - ~o c -. ( ". l 0 rlil.)
"rGtof G'''' (to'" Tn) [.USt-fC I :Ioun lO,1I I l TGH 8'0_11" ,.., (IOU un
,IU'"'" IICISI I ffll Ir CO'.O" (CIPS{ "O.U","1 511014' '101114 (T."t "I)
(IIUSHfO Jlcnus I 1.0 HIICt'" "fI" tollO IIL'U (icyl 1/0) ClU\"'IO
("..tOIL IIUCS Ie - CII 1"1(1) 1 IInslYf. ; :10 Of 1 . Y'IT flUllf
'.""'111';" . hOt-PL.'HIt I (0"0'" '1"'1 .LCIS l"ftOUG"OU' h(j'1l011 1
-II.., "1""( lII'f(tllU. .ORIS 1 1 'flCflll 'III( S£Ofllftrll'UT ftlUINn
)z." I IInDl' FFffIlYF~(E1iI1 C,"Cl) (ONII"UOU5 I .HOL' IUAlI"" 'H- 1.'
('" IIItTh) 1 ""UTIIU' BOUNC""
\0 . ~ 1"1.:) (. -. (lG. ]41 IN.)
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"tRU" nn ""0 bUC' 00" i/O) (I~SHfO ("'."un '''OS 10 - CJI '"1(') .
II"S!.tVt . Sl'\fT . ua'FII"'1.I . 1II0"'51lcn . "O.'\ASHC I Fr"
dftf ~(jOTS 1'1'I'OUIiHOUI HOltlO" 1 ffif fU,( TU"UlII (lJ,nIlfUDUS 'O'U
r~Q.CffH 'IIEO SfOIIlUU" fIllG"''''15 >1 "" I IInCL' fffU"fSCU' (MCL)
collt"..unU5 ; 'ILOl' ILlIlI"-'l 'H- 1.6 ('H III(tUt) ~ ..ll1l11n ICU"O."
~:II:~ - 1(") (III. (H - "....)
llG"' toP" (10" 711) C'US"fl) 1 LtI'" U"'C ~ lIG"' 81OtItIIU" 'U' (IOU HZ)
C;IIUS"IO IIICIU J LIGM' G'''' (HU 1Il) C.Us..,o ; 'ILl 8'0". (lOTI 61)
'.US..FO IIOIS' I .nsnt ; 50ft. un HIIIILf . NOIIISIiCU
040'llIlLIISTlC I fn fl"'f .(lOTS IIIUU(.H(lUI "Ollll'\h . FUr frill:
'UIIULU co..'uunu\ 'OIFS : 10 'flCun -1110 ~fOl.UTl" "".tUS U Jill
-ItOl' fFFl'WF5U"'T (..Cl) COIiIUtrll.[iUS ; .nOLT AlUl1tI1 II*" 1.' ('h flUU) I
/rInl II Fj(Hf ° 1!0U"DAt'
HIII,-IIIN( S'OILS 1If.. (OL'\1I". IIOllllh' 1t"""OfO IIiI U61. lUG. 10/, I'" SOIL 1
HIP . 18.~ C '1 ~D CfI. 0uo's I" C4 '.OLln"'H III snf' CD.l f'I'II'.'S- ..., WE
8:T FI"'F -OOS I" U"fl HAlF OF C2. JlCSS JIlT .I. CJI '''ICI cne-s SU'fICf. ,oClns
OF licn' LOAII ...'tlltll CO"'lSf Ht tF 'IDlUJIF. lCt (GaL 1010£11". Of Oil' IIn£
11;. CC;"Ct-trlIIIIIC IAO"'-5UINIC l O. IIIIOS O.'i '" \/1) Uf ISSOCU'(() ""1'1 COIL '0
,'e''. I..f 1I'.r 15 SfIlIl8TFO FtCJI 'Hf CO'l "' " 1 '" UTII Of!' '''SUJI. A'fFtrIO
(.HL cr'''I''~ "'''1. ... nF 1"1 '~HCTiO (It''' IS 2.1. '"t I.SIOt Df '"I II..r I
175
-------
Table A-28.
Laboratory analyses of 1969-14
soil.
SI;AI~S - - -
- - -F ECLAt "'EO "INE SPOil
J. S. DEPAC:TH!ENT OF AGRICULTURE
SOIL C:JNSEAVATION SEflVIC~, MTse
NATIONAL SaIL SVPYfV LA80PATORY
L INtOl,.., NEBFlA$KA
S~IL CLASSIFICATION-
SOIL NO
- - - - S76MT-G87-11t
COUNTY
POSE8UO
Gf~HAl M~THOOS- - -16, 1818, 261, 28
SAMPLE NOS. 76POb54-16PObf,5
... -- - - ... --- - -- - --... - -----... -- - --- -- --- ---- ------ -- -- ---- ----------... -- - --... -------- ---- -------- -- -- ---............ ------ -----...... ------
OEPT H HOA t ZG"4 1- - PAPTICLE S I lE ANALYSI S, LT 2M"', 3Al. 3 Al At 3AIB - - - IP ATIO
FINE I - - SANa - - - 11- - -SILT- - - -I FAMl I ~TFI PINE NJN- BOI
SAND SILT CLAY CLAY YCOS cap S "'~cs FNES VFNS CDS I HISI YF 51 TEXT II CLAY C03- 15-
2- .05- L T L T 2- 1- .5- .75- .10- .05 .02 .005- SAN~ .2- TO CLAY BA.
.05 .002 .002 .0002 I .5 .25 .10 .05 .02 .002 .002 2-.1 .02 CLAY TO
CM 1- - - - - - PCT l T 2M'" ... - - - - - - - - - -I PCT PCT CLAY
-... --- --- --- --- -- - ---... -- -- -- ---- --------------- -- --- - ---... -- -... - - --- - ---... - - - - -...... - - - -... - -... ---- -- -- --- --------------- - ------
000-001 All "c;.5 35.9 14.6 ., 1.3 2.6 2 B. 7 16.5 12.2 23.7 33.0 1.32
001-002 Al2 52.2 34.0 13. B .3 .9 2.' 33.6 15.0 12.9 21.1 37.7 .61
002-005 AI3 56.0 28.6 15.4 .3 . B 2.1 36.5 16.3 7.3 21.3 39.1 .'1
005-010 CI 60.2 29.6 10.2 ., 1.1 2.7 1t3.5 12.5 11.3 IB.) '7.7 .o~
010-050 C2 78.7 16.0 5.3 .1 .' '.9 59.7 13.6 '.2 11.8 65.1 .'7
050-100 C3 81.4 13.7 '.9 " .2 3.' 65.5 12.) 3.8 9.9 69.1 .>7
100-200 C' 86.6 5.3 B.I 9.' 71.5 .37
000- 0 05 I AI
COAL
COAL
COAl
COAL
- - -- - --- - - --- - - - ------ - - -- -- ---- ----- - ----- - ----- --- - ---------- -- - -- - -- - - - - -- - -- -- --- --- -- -- - --- - -- --- ------ - --------
CM
(PUTlne: sIZe ANALYSIS. 111M. 3B. 381. 3B2)( BULK DENSITY
VOL. 1- - - Wf1GHT - - - - - - -J "'10 4A1H ..01
GT GT 15-20 20-5 5-2 IT 20-2 1/3- OV~I" COLE
2 15 .014 PCT IUR Opy
PCT PCT 1- - - PCT LT 75 - - - I L T20 G/CC G/CC
)t- - - -WATf.Q CONTENT-
'BI C '81C 'B2 'Cl
1/10 1/3- 15- ..0
8AQ BAG PAP CHI
PCT PCT PCT CM
-I CARBONATE
b~!B 3A1A
L T L T
2 .002
PCT PC f
I--PH--I
8CIA 8Cli
III 1/2
H20 CACL
')fPT-4
- - -- - - -- - - -- - -- - ------ - --- ---- ------- - - ---------- --- ---- -- --- -- --- ---- --- - ---- - --- - - -- -- -- -- - - -- --- - ----- -- - -------- ----
000-001 2 0 0 2 3 1.2 B 19.3 10 7.' 6.9
001-002 2 0 0 2 3 1.3 B 8.' 11 7.3 7.1
002-005 2 0 0 I' 16 1.3 B 6.3 12 7.3 1.2
005-010 5 0 I , 9 1.3B 1.1t1 .020 16.5 0.6 .13 3 1.2 7.1
010-050 I 0 0 T~ I 1.66 1.61 .002 9.' 2.5 .11 10 8.0 1.1
050-100 2 0 0 I 3 1.6 B 2.3 II 8.1 1.6
100-200 6 0 ' 2 5 I.H 1.1t8 .002 9.9 3.0 .10 10 1.9 1.6
000-005 1.30 1.39 .023 IB.3
- - - - - ---- - ---- --- ----- ----------------- ---------- ---- --- --- -- - - - - - --- ---- - - - -- - - - - -- - - -- - - -- -- -- - -- - --- --------- ---- ----
''HEPTH tORGANIC MA TTFR I IPON PHOS 1- _cXT-ACTABLE BASE S 5RltA- -I 6(1Y AL (CAT ~xCHI Fo:AT I,) ..TtO CA 1 BASE SAT I
bAI A 681A ClN 6(28 6~2-: 6020 6P2B 6028 6~1A 6G IF 5AJA SAbA BOI 803 5F! 5C3 5CI
ORCN NITG EXT TOTl CA "G NA K SUM 8ACl KCL ~XT8 NHAC NHAC CA SAT EXTB NHAC
CUB FE f xTB TEA EXT ACTY TO TO NHAC ACTY
CM PCT PCT PCT PCT 1- - - - -MEO I 100 G- - - - - - I CLAY Me peT PCT PCT
-- --- - --- ---- -- - - -- -- -- --- -- ---------- --------------------- - --- --- ----------- -- -- -- --- - -- -- -- - ---------- --- --- ----
000-001 6.26 .299 21 5.' TP .6 2'.3
001-002 2.63 .110 H '.8 .0 .3 12.3 .89
002-005 1.82 .068 27 '.1 TP .2 9.1 .59
005-010 2.'3 .082 30 '.B TP .1 13.3 1.30
010-050 .26 .018 I' '.6 TP .. 3.&
050-100 .27 .013 21 3.1 TP .1 2.5 .51
100-200 .'6 .021 22 ,.) TO .1 ).B
JOO-005
- - -- - -- - - - --- ---- -------------- ---- - - - --------- - --- --- ------- ---- --- -- - ------ --------- -- - - -- ---------------------- ----
DE PTH CS.tTIJflATC:O PASTEl NA NA SALT GYP (- - - - - - SA TURA T I ON EXTPACT dAl- - - - - - 1 ATTEP3F.RG
8El 8CIB BA 502 5f 805 bF lA BAIA 6NIB 60lB 6P IB 60lB blU 6JlA 6K lC 6l1C 6MIC &FI "2
HST PH H20 ESP S" TOTI EC CA MG NA K CO! HC03 CL SO, NQ3 LOla PlST
011"- saw -'"HOSI LMn INOX
CM CM PCT PCT PPM PC T CM ( - - - - ,..~o I LI no - - 1 PCT
-- - - - --------- -- ------ --- ---- --------- ------ ---- --- ---- ----- -- -- - --- - - -- --- -- - - -- -- - - -- -- -- -- -- - ----------- ------------
000-001 6.1 87.0 2000 0 2.50 25.1 8.5 .1 1.8 .0 13.& .6 11.6 .0
001-002 6.8 40.1 970 0 2.65 27.' 9.3 .0 1.1 .0 6. B .9 28.8 .0
002-005 6.8 36.0 1100 0 2.99 35.' 9.5 .1 1.0 .0 6.1 .B 38.6 .0
005-010 6.6 3&.5 990 2.9B 33.5 10.5 .1 .6 .0 &.2 .6 &5.0 .0
010-n50 7., 28.4 970 3.3T 26.6 2b.4 .2 .. .0 2.0 .2 5..5 .0
050-100 2200 1.6 28.6 560 2.19 12.1 11.) .3 .3 .0 ., .3 31.3 .0
100-200 1500 1.' 21.8 890 3.11 2&.8 2&.0 1.1 .) .0 ..1 .3 51.6 .0 NP
000-00'5
- -- - - ---- - - - - - - -- -- -- - ---- -- -- -------- --------- -- ---- --- ----- -- ------------- -- ---- - - -- -- ---- -- -- - --- ------------ ---- ----
1&1
I BI
CLOD OF All, A12. AND A13 FQFI BULK CENSITY AND MOI$T1JH PETlNTION.
ESTI MATE
176
-------
A 11
A12~
A13-
C1-
C2
C3
C4
~
,.
,
, .
."
.,#oJ
.
. .
~
.l
.O'\, .~
\ . ,
, .
. \
.120.
4
~ .~
'1{ '.":;r
. 'i').r;,..~
.--"i'..1
- I
Fig. A-14.
Photograph of 1969-14 soil profile.
177
-------
Table A-29.
lOll SUItU
Pedon description of 1970-15 soil.
SUII'" SII'U 110.1 CI I JJ 11
LCUUOU IIF 1/4. ., 114, SV 114. SH1 n IUI, '4If, . -. If Of (Duno. .,.
CLUSlFIUflOII'
nn "tUS
IIn 110.' II IS
su'" ..
'II U8'UUUU
SUL HfI""'U.'
.nu "'UI
"1(1"'''1081'
'''''lIlun-
''''SIO''''''''
'.UDIEl I'"
""ttun..
'..n, ... fI ilL I
"0111011
. II
. "
. IJ
",UIU
nun.tIIIl .... ..,I(IS 1I0tI'.. ,U.LtDI AUIun
".'1 COIIUWI .,,'CI, SDUINUn
SV"U' .. "SitU' .''''U. l4 DIIIUS .
'.'UI DUlfn , unit. Df'UU ,
flO"'" .,,'uu . nOI "UUI UIU
can'OL SferrDII LUlU ..- U"U. In CI UtI[l1 1IC U
auuuI tuSU -UL 011 1 IIf 0
no.... ss r cun .
COU.'''' Iff 'U'KS
u.uu ""'U SLOPI""
"""UI\I u DtCoUU ,
."flIun' DlCoUES f
0"'"' C'.
HO'Ili.
'ODfIUU\' U'ID
U'HL n. ulllouuru, u'u"os
011 S\DH
,u nn "0 Fa'"
SLHM"'t IdU'U:IfD UllCOUOUDnu '.11'11\ net.un
CUU'f.OUS 51110110" "0 tlLtlnGUS SUUTa.'
"'''ILI OIIU.,'IOII
o - I ". ( c - a HI.)
'HllO"Uiol ,,0"111 UOU S/4) U\lSI'ft I ,tilt ".0' LOU I 01. nunUtli 1101111
\tun 4/4) 'IUS..,C 1I0tn I tlfoIl 'III' i"""L" "'U"\I" I SOl"
nl, "JUL' . 1I0Ilnt,..,. . 1I0ItPUS1I( I ...., PlU IIIOTS
""ED 'IOUIIO SlO.U '"0 '..IUS' 'A'" flWI lI.,i""A. I!;IUS
-oaunfl' f,F(lnset.' (tf(L) c:onuuau~ ,'Dllnn,LY IUIUIU ,... I.a
UlkO~'''''Cl HUt) . """"'" 10""'''111''
I'" l [III. ( C. I III.)
HUO"IS" 110"" ((0" 5/U (tUStlfD I ,...,
(1091 4H) '.UStlfD ,on, . ..foil 'Ut
HI' ,11: lieu, "oUTlCI' . "O..,,,ISlI[
-UHO III:OU"O STOIiIU '''0 'HIUs . 11-".'
IIODfIUH' 'ffUYESCflll (flU) CO"'l1"'UOUS
UIO_'tlnOL nUE) I 11ll1l1n leu-un
l - \ C-. ( I'" 2 1-.)
"LlO'US.. (!tOWIil (Uti "" CIUSIilU I '1111' 51110' LUll I 01, ""UtlUM '10".
(10.. "H) UUStlU IIOIU' I tI,n fll10f GU"UL" S""'fUII I 10"
Yf" ".aIU . 1I0iluren ,lItII'L'StIC I IIU' '.1. 100U
."'H "011110 n'lu ilia "UUS I ".., '.11' UI"..' nllS
IODUUH'Y ....,uusu"" (tieL) conuuous . loountLy .unlll' ,..- 1.1
I.IIO"''''''l(ll IIUU . 1"1.1" "all' InUIIO'"
Sill" LOU- . 01. 'ULCillStI 110""
'..IIUUI Inu"u" I 10"
I "II' "., 'GOTS
fill' "'UUL.I .oilS
. IICOflnfl' aLIiUNI 'to- I.l
,... 10 CI. ( 2 - 4 111.)
lIfi'" UO""UH GU' (10" tn, (lUSHIO . '111' S"DY LOlli I 110.. (lOYI un
c.'US..u IIOIST f .181 ,un "IUCIUI( . urcuu ""0 .
WU' "UIl'E ,IIOIlU1tU ,-nilUSTlC . -.., '.11' .oon
IUTnf't IUUIIO STOIIU '"0 'U'LIS I CO_IIOII "III IIIUUL" 'tlrs 1'118
UlUTO..t ""'lItIII1S )2 ell I IIDOUUU'Y I:ffUnSCU' (MtL) CO., "UOUS I
.00Uilfl' IUILUf ,t'- I." (fI'O'H'IICl flLVi) I nUTla" IOUIIIC,.,
10'" 'W) C-. ( ,- 1O II.)
LI,H' GU' (10" HU (lUSHU 1 SUOf LOU , 'IU IIOWII (10n II» ClUSMU
IOrs, I 10 'UeUI nn ...111 51"0' LOlli ttuown.. "0.' <10tl '''' ClUlllfG
'ou£tS O' c.OllnutJlICi II"UUU' ... ell 'HI(I) . IItlSsn' . untl'LY MIlD
F'UIIIl£ . lIallsnc" ,IIO.'USHC I COIIIIO.. FIliI JOOYS
'''OU{,M
-------
Table A-30.
Laboratory analyses of 1970-15
so il .
SOil CLASSIFICATION-
S'RIES -
SOIL NO
-OEVEGETATEO MINE SPOIL
u. 5. ')EPARTM":NT OF AGRICUL TUR.E
SOIL CONSEPYATJON SCFlvtCE, MTse
NATIONAL SOIL SUF:V~" ltlBOfjATO~'r
l INCOL'~I NEBRASKA
- 576MT-081-15
r:our\nv -
ROSE8uO
GPoIt:ft At "ET~OOS-
-lA, 1818. 241. 28
SAMPLE NOS. 76P0666-7tPOb74
- -- - - ------------ ---- --- ------ ------ - -------------- --- ----- - - ---- ----- - - -- -- - -- - - - - - - - - - -- -- -- - -- - --- -- -- - - - - - -- -- -- --
I)EPT H HOR ! ZON (- - - - - - - - PART! ClE SI ZE ANALYSIS, 1 T 214M. 361, 3 "1 At 3A16 - - tPATtO
F tNE 1 - - SANG - - - 11- - -SIL T- - - -I FAML pHR FINe- NON- 801
SA NO SILT CLAY CLAY VCOS CORS MH'S FN'E~ YFN$ COS I FNS I '/F SI TF XT II (LAY (03- 15-
2- .05- IT 1 T 2- 1- . S- .25- .IQ- .05 .02 .005- SAND .2- TO CLAY 8A'
.05 .002 .002 .0002 1 .5 .25 .10 .05 .02 .002 ..002 2-.1 .02 CLAY TO
CM 1- - - - PCT IT 2MM - - - -I PO PCT (LAY
- -- -- -- -- ----- ---------------------- - --------- ------- ---- -- - --------------- - -- - - - - - -- - - - - -- --- -- ------ -- - - --- - - -- -- --
000-001 All 18.4 15.6 6.0 .2 .6 2.1 54.2 21.3 12.0 3.6 57.1 1.12
001-002 A12 81.4 12.1 5.9 TR .2 1.5 53.0 26.7 9.5 3.2 S4.7 .11
002-005 Al3 56.8 38.3 4.9 .1 .2 .° 31.0 18.6 32.2 6.1 38.2 .67
005-010 Cl 65.9 26.0 8.1 .2 .3 1.5 '+0.9 23.C 11.4 14.6 42.9 .36
010-050 C2 60.4 30.3 9.3 .2 .6 3.1 37.9 18.6 12.1 18.2 41. B .30
050-100 C3 11.2 21.5 1.3 .2 .S 3.5 46.2 20.8 8.6 12.9 50.4 .45
100-200 C4 66.2 21.3 6.5 .2 . T 2.6 3 B.2 24.5 16.8 10.5 41.7 .5S
100-200 SHAlE 1.9 64.4 21.7 1.4 <.1 1.0 2.1 1.3 6.1 58.:3 6.6
100-200 SHAl E
-- ------- - --- - ------------ ----------- ---------- --------- --- - -------- --------------- -- -- -- -- --- - -- -- ------ --- - ---- ----
!)fPTH
CM
IPA~TICl~ size ANALYSIS, H", 38, 381, 38211 BUlk DENSITV
Val. 1- - - Wt:IGHT - - - - - - -) 4AI0 itAIM 401
GT 6T 75-20 20-5 5-2 LT 20-2 1/3- Ol/fN COl~
2 75 .071t PCT SAP ClOY
PCT PCT (- - - PCT LT 75 - - - 1 LT20 G/CC G/C(
1(- - -
..BlC
1/10
8..
PCT
-WATEP CONTENT-
4~ lC 4B Z It!: 1
1/3- 15- ~~o
eAR 6AP CMI
peT PCT eM
- - -I
CAPBG"ATF
bilB 3Al~
l T l T
2 .002
PC T PC T
«- -PH - -I
8(lA 8CH
III 1/2
H70 CACl
- ---- - ---- -- -- -- ------ - -- - - -- -------- - ----- - - - -- - -- - --- -- --- - - - -- - -- - - -- - - - - - - - - - - --- -- --- - - - - - - - - --- - - - - - - - - - - - - - - - --
000-001 0 0 0 0 0 0 10.3 1.3 7.1
001-002 TR 0 0 0 TR TR 4.2 B.O T.5
002-005 1 0 0 1 TR 1 1.3 ' 3.3 8.1 7.5
005-010 2 0 0 2 1 3 1.4 ' 2.9 12 8.3 7.6
010-050 1 0 0 TR 1 1 1.6 A 1.70 .011 9.6 3.5 .08 15 8.3 7.3
050-100 5 0 TR 3 5 8 1.5 A 3.3 l' 8.5 7.1
100-200 2 0 0 1 3 4 1.65 1.67 .004 10.~ 3.6 .11 16 8.4 1.7
100-200
100-200 1.28 1.38 .025
- ---- ------- ---------- - --- -- ---- ----- - -------- - -- -- - - - - - - - --- - - --- - -- - -- - - - --- -- --- -- - - -- -- - - -- - --- ---- - - - - - - - - - - - --
O'=PTH 10RGANIC "'ATTER 1 I ~ON PHOS 1- -EXTRACTABLE 8ASES 584A- -I ACT V AL I (AT EX(HI DAT 1(1 1" T 10 CA C 8A Sf SA 11
U1A 68LA Ct" 6C28 6N2E 6020 6Pze 6028 bHIA bGl~ 5A3A SAbA BOI 8D3 5<1 50 ')r:l
ORGN NI TG EXT TOTl CA MG NA . SU. 8At:l '(L EXTB NHtJC NI--4AC CA SAT [XTB NHAC
CAR8 " EXT8 TEA ':XT ACTY 10 TJ NHAC ACT V
CM PCT PCT PCT PCT 1- - -M'=Q I 100 G- 1 CLAY "0 PCT peT '(1
-- - -- ---- - ---- - -- ---- -- -- - --- - - -- - - - -- --- ----- -- --- - --- -- ---- - --- - ------ - - - -- - -- - - - -- -- - -- -- -- - - - - - ---- -- - - - - - - - - - -- --
000-001 2.24 .178 13 2.7 TR 1.3 6.1 1.10
001-002 .83 .081 10 2.5 TR .4 4.4 . 7~
002- 0 05 .80 .055 15 2.9 TR .3 4.2 .85
005-010 .30 .023 13 3.8 TR .1 3.1 .3B
010-050 .16 .018 9 4.7 .0 .1 3.4 .37
050-100 .11 .018 6 4.6 .0 .1 2.7 .37
100-200 .13 .018 7 5.4 TR l' 3.0 .46
100-200 .24 .021 11
100-200
-------------------------------------------------------- --------------- -- -- --- ---- --- - -- -- ------ ----- --- -- -- -- - -----
OE PT"
I SATURAT~D PA STE 1 NA NA SALT GYP 1- - - - - - SA TUP AT I ON ~XHACT 8A1- - - 1 ATT~,"BEr.G
81;"1 8C 18 8A 502 5E 805 6F 16 8Al A 6N18 b[1l8 6P18 bel B bllA bJl A bKlr: bll C bM lC "1 4'2
ReST PH H20 ESP SAR TQTl EC CA I~ (. :~:. . C03 He03 CL S04 N03 lQ10 PlST
OHH- SOlU MMHOS/ L"IT I NOX
CM PCT PCT PPM PCT CM ( "EO I 11 T':J: - - - I PCT
CM
- ---- ----- ------ ------- - -- --- ------- ----- ------ ------ ------ ------- -------- --- - ---- - ---- --- - - -- - -- - -- -- - -- -- -- - - - - --
000-001 6.4 58.1 2000 3.34 33.1 10.b .1 9.8 .0 1.5 4.1 2.5 .0
001-002 7.3 38.3 450 1.50 12.6 3.9 .1 1.1 .0 13.0 1.1 .6 .0
002-005 1.3 32.5 330 1.26 10.5 4.2 .1 1.1 .0 9.5 .1 1. J .0
005-010 1.6 26.8 130 .69 4.8 2.2 .1 .6 .0 4.7 .4 .6 .0
010-050 .208
050-100 1200 8.3 .208
100-200 3000 8.1 29.9 290 1.30 4.2 ".j 1.j 14.:;) 21 3 C
100-200
100- 200
-- --- -- ---- - - - - - -- --- -- -- -- ---- ------ ----- - --- -- ------- - --- --- ------- - -- - - - -- - - -- - -- - -- -- - - -- -- --- - -- -- -- - - -- - - - - - ----
1 A 1
( 81
1 C I
ESTIMATE
1:2 SIOl WU'R RATIO
BY SOIL MECHAN1CS lA80Q.ATORY, USDA, LINCOLN, N~.
179
-------
A 11
A12~
A13-
C1--
C2
C3
C4
..
Fig. A-IS.
Photograph of 1970-15 soil profile.
180
-------
APPENDIX B
Water l10vement
18 sId. dev. 1.34
sId. dev. 3.88
15~:~
12 ~
9
~:
6
3
~
1- Native Range' Chinook
2-Native Range' Yamac
o
o
4 .8
I 1
12
1
16 20 24 28 32
I I I I 1
......
...
~ 18 sId. dev. 227
.......
E
~ 15
~ 12
!:i
a:: 9
~
LL: 6
z
sId. dev.I.02
~~
~~~
3
o
4-Native Range' Kabar
6 - Native Range' Busby
o
KEY
REPLICATION
I 0--<>-0
2
-------
o
18 Std. dev. 2.60
StrJ. dev. /.36
:;G~
~
&,..--"
<0 ~
6
3
3-01d Spoils' 1948
5-01d Spoils' 1924
o
o
~ 18 Std. dIN 2.7'9
"-
5 15
z 12
Q
~ 9
a::
~
u: 6
z
Std. dev. 0.48
c
c
'C
~
- 3
o
7-01d Spoils' 1924
9- Old Spoils' 1924
o
9
6
KEY
REPLICATION
I 0-0-0
2~
3 0-0-0
18 Std. dev. 3./8
15
12
3
o
10- Old Spoils' 1932
Fig. B-2.
Infiltration vs. time measured in old spoils at the
Colstrip study area in August, 1976.
182
-------
.E 18
......
E 15
u
z 12
Q
~ 9
~
~ 6
u..
~ 3
Fig. B-3.
o
18
15
Sfd. dev. 1.88
I:~
3
o
II-New Spoils' 1975
o
4
sfd. dev. 2.78
~~
13-New Spoils' 1972
o
o
18 sfd. dev. 3.14
~~ci
15
12~
~
~
o
o~
Q
r:r
9
6
3
o
15-New Spoils' 1970
sfd. dev. 2.50
-------------
::
:~
12-New Spoils' 1973
14-New Spoils' 1969
o
KEY
REPLICATION
I~
2~
3 o--o--c
Infiltration vs. time measured in new spoils at the
Co1strip study area in August, 1976.
183
-------
Table B-l. Volumetric soil water content (%) at selected depths in natural
soils near Co1strip, Montana.
Native Depth 1976 1977
5011 (em) 6/9 6/29 7/11 8/11 8/24 9115 10/22 11/24 1/15 2/12 3/13 4/6 4/14 5/2 5/15 5/29 6/15 7/8 7/19 7/)1
15 21 18 10 05 09 06 10 13 25 32 23 31 20 09 15 22 14 07 06 04
30 26 " 17 10 12 10 09 14 18 26 27 34 25 17 20 24 19 11 10 05
45 26 27 21 12 13 11 10 13 14 18 26 34 28 23 24 24 20 13 12 II
60 27 28 25 14 15 14 12 14 14 16 27 J4 29 26 25 25 23 15 13 13
Chinook-l " 28 1'~ 27 16 18 16 15 17 15 18 27 J2 31 27 27 26 25 18 17 15
90 30 J! 29 20 23 19 18 20 19 20 27 30 31 29 28 27 27 21 20 19
120 28 30 29 24 29 24 22 24 21 22 25 26 31 28 31 27 27 25 24 23
150 33 )4 34 30 " 32 27 31 27 27 29 30 31 31 29 31 31 30 28 29
'80 30 " J2 28 31 29 26 29 25 26 26 27 30 28 30 28 28 27 26 27
210 31 J2 31 29 29 32 26 30 26 27 27 28 28 29 28 30 30 29 29 30
240 29 30 30 28 31 28 25 30 26 27 27 27 25 28 27 29 29 28 28 28
15 33 38 27 26 18 18 25 30 37 41 37 19 34 31 27 18 17 16
30 37 .2 36 26 24 .. 23 30 38 41 33 J2 35 35 31 24 21 21
45 38 .1 37 29 26 26 25 28 37 40 39 34 35 35 33 26 24 24
00 39 42 38 33 30 30 29 32 36 40 39 35 37 36 36 29 26 27
Boxwell-/, 7\ 40 42 39 37 35 35 34 38 37 " 40 35 39 37 38 33 32 33
90 41 43 .0 40 36 39 36 41 37 42 41 36 39 38 39 37 35 37
120 40 42 39 40 37 39 38 41 36 41 40 35 36 38 38 39 38 39
150 38 41 38 38 36 38 32 38 33 37 38 34 36 36 36 37 34 37
180 38 40 37 37 35 36 31 37 32 33 36 33 34 35 36 35 34 36
210 " 39 36 37 36 35 30 36 31 J2 34 32 32 34 34 34 33 34
" 29 23 20 22 23 26 48 38 42 39 23 32 31 31 25 21 20
30 J5 27 25 26 22 27 46 38 42 40 36 34 35 31 26 24 26
45 36 28 26 26 22 26 44 36 42 40 38 36 35 32 26 24 26
60 38 30 26 26 " 26 43 34 ., 39 38 36 36 33 28 26 28
Ethr1dge-4 75 37 29 25 25 " 25 38 30 38 37 38 33 35 32 29 26 29
90 34 29 26 25 20 25 33 27 30 32 34 31 32 30 29 27 29
120 28 27 25 25 21 24 29 22 24 25 25 23 25 24 25 24 24
150 27 27 25 25 21 25 28 22 23 22 23 21 23 23 22 22 23
180 25 26 24 25 22 25 28 22 23 23 21 28 21 21 23 2J 23
210 31 Jl 29 30 27 30 34 27 28 27 " Jl 27 27 28 28 27
15 13 16 10 03 05 04 11 12 21 29 19 28 21 14 11 14 14
30 19 23 16 07 07 09 09 " I' 24 21 " 24 1" 2" 2n 14
45 29 21 19 11 10 07 09 IS 16 17 19 30 25 23 17 2n 16
60 21 'n 21 15 14 In 12 13 16 17 17 28 25 2J 20 19 18
Riedel-6 75 24 22 2J 18 18 14 19 15 18 18 18 28 26 26 21 20 26
90 27 23 24 20 19 17 17 18 19 19 19 25 26 28 22 22 28
120 27 24 27 23 22 19 17 18 21 21 20 21 25 28 24 22 23
ISO 30 26 29 25 25 22 21 21 22 23 22 22 25 29 25 24 25
180 33 29 32 27 28 24 22 2J 25 25 28 23 25 30 27 25 26
210 40 36 40 34 J4 26 25 24 28 30 27 27 28 33 31 28 31
240 37 36 34 33 33 31 30
15 17 15 07 04 03 03 06 11 14 32 17 2J 17 -4 10 14 08 06 04 03
30 21 21 14 09 08 07 06 11 11 27 19 26 20 13 15 18 14 09 07 06
4\ 24 23 19 12 11 09 08 11 10 25 20 29 2J 18 19 21 17 11 10 09
60 27 26 22 14 13 11 09 13 11 22 20 31 26 22 21 2J 19 13 11 10
Chinook-lS 75 26 25 22 15 13 12 08 13 11 17 17 27 25 23 19 21 19 15 13 19
90 26 23 22 IS 14 12 10 13 11 17 14 21 23 21 23 19 17 15 13 12
120 30 30 30 26 23 19 16 20 18 20 21 21 24 24 22 23 22 19 17 15
150 28 28 29 25 23 20 15 20 19 20 19 20 20 21 18 22 21 22 20 21
180 25 25 25 28 21 19 13 19 17 19 17 17 18 18 27 18 18 19 19 19
210 25 25 25 23 22 19 15 20 17 17 17 18 18 17 16 17 16 27 16 18
240 23 2J 23 22 21 19 14 19 16 18 17 74 17 17 16 17 16 17 17 16
184
-------
Table B-2. Volumetric soil water content (%) at selected depths in old
minesoils near Colstrip, Montana.
Old Depth 1976 1977
spoil (em) 6/' 6/29 7/11 8/11 8/24 9/15 10/22 11/24 1/11 2/12 3/13 4/6 4/14 5/2 5/15 5/2Q 6/15 7/8 7/1Q 7/]\
15 21 20 15 07 07 07 12 16 27 36 25 20 27 10 l' 19 27
)0 2) 26 20 1) 12 12 10 16 18 24 " )1 28 ~4 20 " 23
45 22 24 20 12 11 11 0' 12 12 15 19 2' 27 25 19 " 21
60 22 2) 20 12 11 10 08 11 10 12 12 24 25 2) 81 .. 18
1928-5 75 22 21 19 11 10 10 10 10 0' 10 0' 17 11 22 17 19 "
'0 2) 21 20 11 10 10 08 10 10 11 0' 14 15 19 14 17 1)
120 27 25 24 14 1) 1) 10 1) 12 1) 11 11 12 14 10 l4 1)
150 22 21 20 11 10 10 07 10 10 11 0' 10 0' 10 07 10 10
180 11 12 12 0' 08 08 06 08 08 0' 07 08 08 08 07 08 08
210 08 0' 0' 0' 08 08 06 08 08 0' 07 08 08 08 07 07 07
15 14 10 06 05 04 08 12 1) 20 32 2) Jl 20 1) lh 19 17
)0 2) 19 10 11 10 10 1) 16 16 23 2) )2 28 28 18 !5 1R
45 24 20 14 12 11 10 12 12 12 15 19 )0 27 )2 19 " 19
60 24 21 15 12 12 0' 12 12 11 12 15 24 24 )J 17 " 19
1928-7 75 2) 20 14 11 10 08 10 11 0' 10 10 15 17 27 12 20 lh
'0 21 18 14 10 0' 08 08 0' 08 0' 08 10 12 19 11 14 1)
120 21 20 14 11 11 10 10 11 0' 11 0' 10 10 14 10 11 I'
150 21 20 15 14 1) 11 12 1) 12 1) 12 12 12 15 11 11 12
180 19 19 18 15 14 1) 14 15 1) 14 12 1) 1) ,., 11 1) 1)
210 17 17 18 16 15 1) 14 15 14 15 1) 14 1) 10 l2 1) 1)
240 16 16 17 16 16 14 15 16 14 15 14 l4 14 14 12 14 1)
15 16 18 10 07 06 00 0' 15 20 2. 22 28 2J 0' 14 10 1)
)0 20 2) 17 1) 11 11 10 15 17 17 22 ;:4 25 19 21 18 1)
45 20 2) 19 14 11 11 10 12 14 14 20 28 24 21 18 .. 17
60 20 22 11 14 11 11 07 11 12 14 17 2h 29 21 19 27 17
1928.9 75 2l 2) 20 15 12 12 07 12 12 1) 15 2J 2) 21 19 21 18
'0 22 2) 2l 16 1) 12 10 12 12 12 15 20 2l 21 20 21 1R
120 2) 24 2) " 15 14 10 14 1) 1) 14 19 18 18 19 20 1R
150 24 24 24 2l 17 16 10 16 15 15 15 17 19 19 18 19 18
180 24 24 24 2) 19 18 12 18 17 17 lh 16 18 20 17 18 18
15 28 )) 20 0' 08 07 12 18 2) )8 28 )9 )) l' 24 " IQ 12 0' DB
)0 30 50 26 15 1) 11 11 17 20 )J 28 )9 )5 )0 26 )0 .. 17 1J 13
45 29 )5 27 17 16 14 12 16 16 25 24 J6 J2 )0 24 29 2J 18 16 15
60 28 J2 25 18 17 15 lQ 16 14 23 20 29 29 27 22 25 22 18 16 "
. 'I.'~ ~ I '1 75 26 ,. " 18 " ]5 1) " 10 OJ 17 20 2J 21 20 21 20 " 1',
'0 27 29 25 2l 20 17 " 18 15 2J 18 19 20 21 20 11 20 18 lh 17
120 27 30 26 24 2) 20 17 2l 18 22 20 20 20 20 18 20 20 20 19 19
150 24 26 24 24 24 21 19 22 18 22 19 20 19 18 18 " 19 19 18 "
180 2l 2) 2l 22 22 20 16 21 18 21 19 19 19 12 18 19 19 19 18 "
210 2l 22 20 22 2l 20 17 21 18 2J 19 20 19 19 11 19 19 19 18 18
240 " 20 " 20 20 " 16 20 17 12 18 19 18 19 "
15 )J 21 22 20 28 )0 J8 " 44 " 45 27 )7 J2 11 26 24 20
)0 42 )7 )7 )) J5 )7 J9 52 4B 5) 51 42 45 42 41 )5 )) J2
45 40 48 46 4) 4S '" 41 57 50 59 50 " 54 4h 45 " J9 40
60 52 52 50 47 41 50 48 56 42 " 57 57 48 52 " 47 45 48
1948-) 75 46 44 4J 40 )8 4J 41 51 46 47 " SO 47 4h 4) 41 )9 41
'0 48 49 47 44 4S 48 46 54 48 50 \0 49 5) 4h " 44 41 42
120 53 55 54 49 44 5) 50 56 52 5) " IS 51 5) 10 " 4B "
150 54 55 5) 50 49 5) 45 55 51 54 54 5) 52 II 52 50 47 47
180 48 57 55 51 52 5) 49 60 52 56 54 5) " 52 52 48 46 4B
210 49 63 6J 57 51 6J 59 6J 59 59 61 61 OS 60 hl 5' 57 59
240 40 52 51 47 45 49 47 49 47 47 58 49 51 48 49 47 " 4h
185
-------
Table B-3.
Volumetric soil water content (%) at selected depths in new
minesoils near Cols trip t Montana.
1976 1977
Now Depth 4/' 4/14 5/2 5/15 5/29 ./15 7/8 7/19 7/]1
~poll (C8) '1' 6/29 7/11 8/11 8/24 9/1) 10122 11/24 1/15 2/12 JIB
15 27 J6 2] 17 17 17 18 22 2. 42 31 ]8 J2 21 28 2. 25 18 15 14
]0 ]) 41 30 2] 27 22 21 23 25 41 ]3 79 ]5 29 ]0 29 28 24 22 20
45 J5 44 J4 27 25 25 22 24 24 37 ]) ]8 J6 ]) ]I ]) 30 26 2] 23
.0 J5 " J4 28 2' 2. 2] 27 24 38 J2 " J7 J4 ]) J2 30 2. 25 24
19(19 75 ]9 48 ]9 7' ]5 J2 J4 29 ]I 44 27 41 41 3. J6 ]) J7 J2 29 27
.0 44 52 42 40 J7 38 27 J5 ]) 45 J8 J6 41 4] 26 42 J8 28 J7 J7
120 ]I J7 ]1 2' 28 " 2. 22 22 ]4 2. 2. 27 2. 22 26 " 24 22 21
150 28 ]I 27 25 24 22 18 22 19 28 21 21 22 22 25 22 21 20 19 19
180 70 72 27 27 2. 24 19 21 21 ]I 2] 27 24 24 24 25 24 25 2] 23
210 2. J4 2. 29 2' 28 2. 24 2] ]I " " " 25 27 2] 25 24 24 27
15 15 17 08 03 02 04 10 10 22 J7 21 ]0 20 40 12 O. 10 06 07 00
70 22 28 18 11 09 09 .0 14 18 27 " 1] 27 18 18 20 15 10 08 07
45 " 28 2] 15 13 12 12 14 14 20 24 30 27 2] 21 22 17 13 11 10
.0 " 29 2. 19 I' " 1] 14 14 20 22 27 28 25 2] 22 19 16 14 13
1970 15 28 29 28 21 18 " 14 14 14 22 21 25 28 " 25 2] 21 17 16 14
.0 29 J2 ]I 24 19 18 15 I' 16 2] 20 27 28 27 24 24 22 10 17 15
120 ]I J2 J2 25 21 20 17 17 17 21 19 20 24 25 21 2] 22 20 18 16
150 30 ]I ]I 26 22 19 18 18 18 19 18 19 21 21 18 21 21 19 18 17
110 27 27 28 24 21 18 " 17 " 17 17 17 18 18 18 18 18 17 " 16
110 25 2. " 2\ 21 20 " 17 16 18 17 18 18 18 18 18 19 18 " 16
15 04 00 00 00 00 08 04 19 2] 12 19 25 01 O. 01 00 00 00 01
30 21 10 O. O. 07 10 15 2] 32 20 ]0 29 11 19 15 08 07 04 00
..') 28 20 11 10 12 12 17 20 28 25 ]6 ]) 22 24 21 12 10 O. 08
.0 )I 25 11 " 17 17 19 22 27 " ]4 ]4 19 27 24 17 15 12 12
19 7 ~ 75 ]) ]0 22 21 2] 18 22 24 26 29 ]) 34 ]I 25 28 22 21 18 I'
.0 J2 30 2] 22 2] 20 22 22 24 28 ]I ]) ]0 ]0 27 21 24 21 19
120 J2 31 26 25 26 20 24 24 " " J1 J1 20 2. 2> 2' 24 12
150 ]1 ]0 ,. 24 26 20 24 24 25 27 25 " 29 27 27 25 25 2] 24
180 29 28 25 24 25 20 22 2] 23 24 24 24 26 " 25 24 24 22 28
210 28 28 " 25 26 " 23 23 2] 2] 25 25 26 26 25 24 27 25 25
240 28 28 27 26 28 22 24 2] 24 24 25 25 24 27 24 2] 24 2] 22
15 2] 14 08 07 09 17 15 22 28 2] ]0 2] 09 17 14 no OJ "5
]C 34 27 16 14 " 16 20 22 " " ]) 29 22 22 24 18 17 16 15
45 37 31 20 18 19 18 20 21 2] 25 J2 70 " 24 25 2" 19 17 16
60 J7 ]) 2] 20 22 20 20 24 25 24 28 " 29 28 " 24 21 20 20
197) 75 ]8 J5 27 24 25 24 2] " 27 " 27 ]1 27 " 29 27 2] 22 22
.0 ]9 ]7 ]1 28 29 24 " 24 27 24 " 29 28 J2 " 25 2] 2] 2]
120 38 J7 31 28 29 27 24 30 ]I 29 ]I ]) 30 J2 " J2 32 ])
150 40 J7 J5 J2 ]) 29 30
15 27 22 19 19 17 26 ]0 41 27 40 28 15 25 18 20 19 14 13
]0 J6 J2 28 29 27 " 28 ]9 31 J9 ]3 ]0 29 ]I 27 26 2] 2]
45 J7 ]5 31 J2 ]0 28 29 J7 " J8 ]5 J2 29 ]) 29 28 25 25
60 38 ]5 ]) ]4 ]2 ]0 ]0 ]5 " ]7 ]5 ]4 ]) ]) " 31 28 28
1975 75 J8 J7 ]4 J6 34 " " J6 ]) J6 ]5 35 3] 34 J2 ]) ]0 ]1
90 78 J6 ]5 J7 35 ]1 ]) 37 3] ]5 75 ]5 33 35 ]) ]4 J2 32
120 J9 J7 ]6 39 J7 ]4 34 J8 33 ]5 74 ]5 ]4 ]4 ]) ]5 ]4 ]4
150 39 ]8 ]7 40 J8 ]4 J4 ]9 ]3 ]5 34 J4 J4 ]5 ]4 J7 ]4 J6
186
-------
Table B-4. Soil temperatures (Oe) for undisturbed soils and minespoils
at eolstrip study area.
---~
~j t.., D. '" om 1976 --_JJA1f;... 5 TCo-- 1'1'7
f./29 7/11 8 11 8/24 9/1S 10/22 J 1/24 l/ 12 1/1 i. S/2 Sin hilS 7"1 ;/j'1 71)1
(.111:-'001(-1 IS 14.9 21.7 12.2 2).4 11,.1 6.8 1.1 6.' 14.'- 20.7 lH 6 U!.h ,." n.h : ~. r
50 15.9 19.0 2),7 25.1 17.6 U 1,j 3.2 13.0 110.2 15.2 19. ~ 22.11 " ' " 2
'0 11.7 11,9 21.5 22.0 18.h II ) 1,9 U 10 8 JI ) I}.Q I/-,:. 14,'. 1I'>,f) I' "
"0 12.0 11.5 18.6 19.5 n.R J) 'I '.1 ',.1 8.1 86 11.5 11.0 I', 1 ~..? I'>Q
\'AHA(.-.2 IS j),9 19.8 21.2 22.7 Ih.I. "., ].0 11.'.> " ', IR.! 24.1 -" 6 >, " :2.11
50 14.2 17.) 21,7 .?2.lj IH-J 111,4 \2 lJ 0 13.9 1:'.7 JR,] 2'1,\ 12 2].2
qo IJ.7 15.4 2J.2 21.7 18,(, 12, 'j 6.' [rI,R II 1 11.7 Ih.l lH ) I 'I,,~ 1'1 I
L50 L2,(1 12,2 19.0 I').j II:I,J 1".2 ' 8 8.:' " " 11.1 11.1 '" I.
1'14R-) " I').J 'I ' 22.7
',0 lH I .'1),1) -. " 22.'1
'0 I':'.'" If',I, 11,1 lH "
"0 1::.11 II [',,7 I', "
192'--) I', 14.7 21.L 2:',\ 2'" 1",4 5.0 \ 0
50 11.9 zn,(J 24.1 24,4 17,1'1 ,., J,')
'0 1),5 19.8 2) 22.7 17." In. ~ '.S
150 12.0 lJ.7 20.) lo.n 17.n 14.4 ".,
IHSIIV-6 15 , 21.2 lJ.~ - ~ ." Lb,'1 \.0 :'.'1
\" 14.9 19.8 22. ~ - ~., 17.8 10.5 6.'
'" 13.5 ]"'.9 lI ' 21.0 1l.'; 1.0
150 12.5 1),0 18,h ]11.'" 17.1 1l..9 I" J
1924-7 " In.1 21.5 21.4 25.1 18." 5.' '.0 11.0.7 20 J I),) I7.J
\0 13.1 2n.o 23.4 24.1 18.8 " , ) 14.7 15.Q ]:'9 19_1
90 12.7 18.1'0 22.7 2J.] 18.8 11.4 U IL5 1),5 I' 0
150 10,8 11.) 18.1i 20.0 18.1, 15.4 10.1 9.1 10.1 " 7 1....1
IIL:SBY-8 15 15.2 22.7 J.l 11.0.'1 20.7 13,11 2'1 5 " 7 11.9 n.]
so 14.9 2].7 24.9 '" 20.) 10. I \.0 11..9 1 ~,h 1'111 2J 21.'1 22.9
'" L).7 111.6 22.9 22.7 20.0 11.S b.' 12.5 11.:' 12.7 1,'. 'J 17.R I',." IM.I
150 12.0 14.7 lO,) ~L"I. 3 19.) 15.4 '.8 9.; ] (I,~, I',.... " 1 '" ,
l'U..-9 15 11..1.0 22.0 25.1 2".1 L8.8 5.4 1.' 1.1 21.';
;0 11,.'1 21.2 25.1 21.0." 1.11.1 '-' U I.) 4.;
91, J).9 18.8 23.2 18.0 11.1.0 5.2 1.8 4.J
150 11.) 11.) .'U, J 20.J ItI.1 ):'.1) 9.1 ).7 5,2
1932.10 IS 12.2 23.2 21.5 22.7 19.0 5.4 I.J ]1.') 111.1 17.0 18 ) J,,', ~/, I 12,2
SO 13.5 19.5 2J.4 24.1 18,1 '.1 J.J 11.7 14.7 14.7 20.1 24." 'J ',
90 12.7 17.3 22.2 22,7 18.6 11.U S.O 11.3 11.5 I) ' 17.J 22.') .'1.0 21.2
150 12.0 13.'1 ]9.'; 20.1 JR.h 11..4 '.1 lJ ' ".A 11,', 11.4 1 'I. ~
22.7 1),2 11>.9 6 ) '-' 11. ~ 1",.9 7, ,. 11 1/'.J !I 7
1975-ll IS 15,1, 20.7 " 1 2'.. 21.7 2'2.1.0
'.4 2.5 11 ' ]',.1, I..'"
;0 12.7 20. J 2).7 l"'.h 19.1 0 lJ.fJ I.." " I .'0 0 '21,11 22.(1
L7.B 22.1 2),7 19.J I'J.M 2.S "
90 12.0 ' I 6 12 0 1",1 '" 1\ 6 " "
1 ')0 11.0 11.'1 20.) 21.0 19.0 IJ9 1.1
25.1 IB.3 10.', S 4 ' " 12.; PL 1 " " 22.'J .") .. 'I .'11 7
1971-12 15 11.5 17.3 22,2 ! 2.0 11.':> \-1.7 17.1 21.() H " .'J '
17.B 21." 22.1.0 11,9 5.1 ) I J
SO J5.4 ]0.1 10.:' ]2.2 1 ;.. ~ PI.J 1"1 ] IM.M
21.0 11.H 8.6 ",.<1 '.A
qQ 10.) 14.9 20,) 7.(1 8.6 110 !L(] 1';.4 I', " 1".4
110 '.J 11.5 16.) 18.8 17." 11.2 '.4 4.2
22.9 15.4 ,. ,., 1.6 4 ' 1 ~ . 2 HI..'I 17.1 224 22. ~ 2 ~. 4 II
1972-I) II 12.0 17 ,B .20. J 12 0 11.2 11.7 17.1 !() 7 " 21
22.0 17.3 '.1 ', n ' " J 0
\0 12.5 16.0 21.2 In, I 10 ', " 2 1;'.0 I> ' l'llj I '~. J
lS.4 211.' 21.5 17.3 10.1 2 1.1
'0 11.B 11,1 U 7 ' " I 10.':, I! ! " 4 15.1.0 I>, I
110 10. S 12.0 17.6 IB.1i 17.3
20.7 1:'.1.0 4.0 110 \8.\ " " 22 7 i'..'i II 7
]9(,9-11, 15 11.0 19.) 22.11 13.') " 9 1'1. " 21.2 21 ' 2:. ~
10 12.0 19.5 II < '" " " '" > II 7 21 ',
on 12.) 19.0 217 .21.5 ]1.0.11 I' " I
150 11.0 1).2 HI,I !tl.h 16.h
22.0 Ih.4 5 7 4.0 J). 9 If, ~ 17,'1 '.0 " I I' 4 17. ~
1970-] 5 15 12,7 20.7 ~.... 4 2 1),7 14.7 11.0.4 l..? JI.7 14.7 11.0,4
SO 13.2 19.1 .21.1 22.7 \9.0 ".1 \1.9 5.2 II ', I ~ n 1). 'I
10 8 " 11.5 12.0
90 12.1 16.M 20. ) 2J.2 19.0 8.6 '-6 '1.3 7.>
\8.1> 11.7 "
110 11.'1 1).7 18 ) IB.6
r,y.:hrometers removed f,'r .:lblnlnA on' l.lllbr.ltlon
"- Denot~'t psychromctrr f.llLurc
187
-------
APPEND IX C
Root Activity
Derivation of the Plant Activity Index
Plant radioactivity is proportional to the amount of 32p in the above
ground portion of the plant
(1)
Thus,
FC = Kl (PQ)
where
FC = Field count
Kl = Proportionality constant (geometry factory)
PQ = Radioactive quantity in plant tops
(2)
Decay of all radioactive substances is expressed by the equation
N = N e -At
o
where N = Number of atoms remaining at time t
No = Original number of atoms present
e-At = Decay constant
A = O.693/half-life (14.3 days for 32p)
Thus the radioactive quantity of 32p taken up by the plant tops from
injected 32p in the soil is the sum of 32p accumulated (PA) during each time
increment since p32 injection corrected for decay.
(3)
PQ =
t = 2
E (PA) e-At
t = 1
where
and
PA = K2 (SQ) 32
K2 = Proportion of total P taken up by
plant tops during some time period.
SQ = Available p32 in the root zone.
roots and transported to
Integrating from tl to t2
t = 2
f (PA) e-Adt
t = 1
(4)
PQ =
188
-------
(5)
-At -Atl
PA (e 2 -e )
-A
PQ =
Substituting (1) into (5) and rearranging
~)
Kl(PA) =
FC ( -A )
-At
2
= PAl
( e
-e
-At
1
)
where PAl is defined at the plant activity index.
This equation can be extended to evaluate p32 uptake by a plant top
between measurement dates by subtracting the residual radioactivity of p32
taken up during previous measurement periods. A modified field count (FC')
can be defined as
(7)
FC' = FC - FC e-At
2 1
where t = t2 - tl
FC' is the corrected field count at time t2 suitable for substitution
into (7). In this case, in (7) t2 would be the time elapsed from injection
to measurement date 2 and tl would be the elapsed time from injection to
measurement date 1.
189
-------
15FJ~:e",~:""n~"'
f1'ySOOSlS
. 11050
46
1!~hr.saDs,s .,//osu
BUSBY SOIL (8)
July 15
August 10
June 27
"'1
BUSBY SOIL (6)
July 14
August 10
365J~
I L I1r ~ H~'''amnv5 /1OIJS~OSIS
E
~
Calorno""lfa IC/I'IgdolrD
15
1966-...
o
500 1000
o
500 1000
ACTIVITY (cpm)
o
500
1000
~ 46
I
I-
~ 76
i'o,:
~ 137
~ 183l
-I
o
POD Scl"'"1t>("9"
I
I-
~ 761
~ I
i5 107
::;:
w
~ 137
(/)
O'a
,
500
I
L
I
500 1000
ACTIVITY (cpm)
I
o
I
500
I
1000
1')',SOPS,s ,011050
Locfuca 5"""010
...1,'t'I'ntS'O (jrocvl'lciJ/us
,-;Ot.va cv~-c "lOa
<.- tv ysops's 0',1/050
5/>p0 CCjmOfLlS tecton."""
E E
~ 46 ~ 46
I I
I- I-
Il. 76 Il. 76
w w
0 0 r
I- PsorOleo escultlnfo I- KOt1I€Y,O C"510ro
i5I07 LOCfuCO 5e,.,,010 i5 107
~ODyron 5,"""" 5,.,,0 COITIOfO
::;: ::;:
W '- OCfvCO stNnolO W
~ 137 Bromvs ,Qpomcus 0::
::J137 5 "po COI'I'>010
(/) (/) Koele"o er,sIara
-------
15
~ 46
I
f-
~ 76
a
f-
r;:, 107
::;:
w
CS 137
(f)
'o~~~e::
151
46ls"PO ",.mo',"
E
~
Me/dafu,> ofl,crnOI,S
I
f-
a. 76
w
a
f-
r;:, 107
::;:
w
CS 137
(f)
0 J'OCuncu wS
LOCfuCO Serr'OIQ
.Jr1e"",s 0 "dc. c,ona
F"90'"" 9'OJCD
':,Ioa 'c'''''O'J
...}r/f'Y" S a J,ac!J?cV'e'o c~s'e"'o'"
::>v~pureu7'l
,""em" a d'o,u~u'u'
..Jde715'O
H 10',-, ff,erno/,s
.,J'r' L'SCOS loslach}o
1000
o
500 1000
ACTIVITY (cpm)
August 10
1924 (7) SPOILS
June 27, ~JUIY 14
'...)".,...,...5,.0 LoY'J I
I 5 ' ] ~:;~:~~ ~
E
-"!
46 ~ ~e~ ,:,:~:' ;~-;,~'~a~:
~,~,~,
i
~
vX,,' ~
I
f-
~ 76
a
f-
r;:,107
::;:
w
CS 137
(f)
~ l-,m
::;:183
1,' "'" a 0-." ~'c""
.J 'r'" <"'u 7 ' . -. -
I.
1.' ',..",,'
,
1000
1
'T T------i-
500 1000 0
ACTIVITY (cpm)
5(,(--
, ,
500 1000
o
c'
~
I 'CD
D \'e '-"~'
I
"t' c ""0
T
1000
! -: ~~.- :: :::
1-""- ," "0""
t--
o 500 1000
ACTIVITY (cpm/
Augusf 9
SI'~
-------
1975 SPOilS 1913 SPOilS 1972 SPOilS
June 27 July 17 AU\lus' 19 J",e 24 July 17 AU\lUSI 9 June 25 July 17 AuQUS' 9
i~'()(,"O"Jm.'''. "f=~
15 ~ So',oo '0" SOISOla "0" A9'0&l"of't en,'a"","
15
E E Ai(y0lJlJf'(YI C"IIOIum ~cOQO 10",,0 :J
~ 46 A...no larva 46 8n#'tusfQl:lO'l'C,"" ] 46 &0,"". '''''''''''1
;!
I ~ I I
... SolJokJ ItQlt M.oocogo '0'''''0
~ 761 ... ...
l1li.,,10"'1 o"'C,ttOh, ~ 76 ~ 76 Ag""PY'O't c', s 'afvm
~ i "g,", '0' ,- '" S'crr>~"'~'"Y)"
0 500 1000 0 500 1000 ' 500 1000 0 500 1000 0 500 1000
o 500 1000 0 500 1000 0 500 1000 0 500 1000 0
ACTIVITY (cpm) ACTIVITY (cpm) ACTIVITY (cpm)
1969 SPOilS 1970 SPOILS
June July 17 August 8 June 24 July 16 Augusl 8
.w."It>IuS o,f,c.nallS F
15 15 ilJf/"OPy'on C"''O","
Sf.pocomata
E 46 E 46 ..ww.ctCOfIOso'...u !
~ ~ A9'oDy'on ,"'.'01",...,
I I 49'00,'0" C""o'vm
... ... A9'OPY'on -11''''flo'''''
~ 76 Il. 76
w M.r1sc,(f,flo,,,' A9'op,,0'" .10"90'"''''''
o 500 1000 0 500 1000 0 500 1000 0 500 1000 0 500 1000 0 500 1000
ACTIVITY (cpm) ACTIVITY (cpm)
to-'
\C
N
Fig.
C-3.
Plant radioactivities measured in situ on new mine spoils at
area in 1976.
the Co1strip
study
-------
Trdu
15
CHINOOK SOIL - 1
4/17
5/1
5/13
5/31
6/15
3825
1829
46
E Trdu
~ 76
:I:
~
Q. SIca
W
I-' 0
\0 ~ 107
W Z
W
~
w
a:
;:) 137
Cf)
cs:
w
~
183
214
o
Fig. C-4.
500
o
500
500
o
500
o
500
o
ACTIVITY (cpm)
7/11
7/19
7/31
o
500
500
o
o
500
In situ plant radioactivities on Chinook-l undisturbed soil at Colstrip study
area - replication 1, 1977.
-------
4/17
SIca
15
Lema
46 SIca 1
1448
E tca
!:?
:z::
.....
c..
w
0
..... 107
to-' Z
W
\0 ~
.c- w SIca
a: ,
::::) 137
(/)
«
w
~
Fig. C-5.
CHINOOK SOIL - 2
5/1
5/13
5/31
6/15
An spp
76
183
214
o
500
o
500
o
500
500
o
o
500
ACTIVITY IcpmJ
o
7/11
500
o
7/19
7/31
500
o
500
In situ plant radioactivities on Chinook-1 undisturbed soil at Co1strip study
area - replication 2, 1977.
-------
4/17 5/1
SIca 1
Trdu
15 Artr
SIca 2
46
E Catl
~
:I: 76
~
~
w SIca
o
~ 107
..... Z
\0 W
V1 ~
w
a:
::J 137
en
«
w
~
183
CHINOOK SOIL - 3
5/13
5/31
214
o
500
o
o
500
o
500
o
500
ACTIVITY (cpm)
6/15
7/11
7/19
7/31
500
o
500
500
o
500
o
Fig. C-6.
In situ plant radioactivities on Chinook-l undisturbed soil at Colstrip study
area - replication 3, 1977.
-------
4/17 5/1 5/13 5/31 6/16
Agsp
Rowo
15 Popr
Agsp
46
E
~
J: 76
~
~
W
0
~ 107
Z
W
~
t-' W
\0 £l:
0\ :J
(/) 137
<
W
~
183
Fig. C-7.
214
1932 SPOIL-1
7/9
7/19
o
o
500
o
500
o
500
500
500
o
o
500
o
500
ACTIVITY Icpml
In situ plant radioactivities on 1929-10 spoil at Co1strip study area -
replication 1, 1977.
7/31
o
500
-------
46
E
~ 76
:J:
~
~
u.
0
~
,..... Z
W
\0 ~
"-J W
~
;:)
U)
<
W
~
,JLapu 1 I I
]Agsp r
~pu 2 3085 1490 J ]
Arlo
Gusa b
Agsp 2091
Lapu
..!. 0 Do 0 500 0 500 0 500
15
107
137
183
214
Fig. C-8.
1932 SPOIL - 2
4/17
5/1
5/13
5/31
7/19
7/9
6/16
7/31
o
500
5
o
500
o
500
o
500
ACTIVITY (cpml
In situ plant radioactivities on 1929-10 spoil at Co1strip study area -
replication 2, 1977.
-------
1932 SPOIL - 3
4/17
Arfr
15 Agsp 1
Agsp
46
E
~ 76
:I:
I-
CL
W
C
I- 107
~ Z
W
\0 ~
00 W
a::
;:) 137
en
C
w
~
183
5/13
7/9
7/19
5/1
5/31
6/16
So Spp
Chvil
Agsp
Kacr
SIca
214
o
500
o
500
500
500
o
o
500
500
o
o
o
500
ACTIVITY Icpmt
Fig. C-9.
In situ plant radioactivities on 1929-10 spoil at Co1strip study area -
replication 3, 1977.
7/31
o
500
-------
15
46
E
S 76
J:
I-
a.
w
Q
...... I- 107
\0
\0 Z
w
2
w
a::
:J 137
IJ)
<
w
2
183
214
o
Fig. C-IO.
4/16
Agcr
Brin
500
o
4/30
5/11
1970 SPOIL-1
5/31
7/20
6/17
7/10
7/31
1492
o
500
o
500
o
500
o
500
o
500
Agcr 1
500
o
500
ACTIVITY (cpm)
In situ plant radioactivities on 1970-15 spoil at Colstrip study area -
replication 1, 1977.
-------
46
E
~ 76
J:
~
Q.
W
C
'" ~ 107
o Z
0 w
:2
w
a:
;:) 137
en
<
w
:2
183
Agcr ~rin 5 ]
]Agda
]Agtr
~Agel
.! .!..
15
214
Fig. C-ll.
o
1970 SPOI L - 2
4/16
4/30
5/11
5/30
7/10
7/20
7/31
6/17
500
500
o
o
500
o
o
500
o
o
500
500
o
500
500
ACTIVITY Icpm)
In situ plant radioactivities on 1970-15 spoil at Colstrip study area -
replication 2, 1977.
-------
46
E
~
J: 76
...
Q,.
w
Q
N ... 107
Z
o W
I-' :I
W
a:
::::)
en
c
W
~
Agel B ~
~lin-1
Brin-2
Agcr -1
.
' . -~
15
137
183
214
Fig. C-12.
o
4/16
500
o
1970 SPOIL - 3
4/30
5/11
5/30
6/17
7/20
7/10
7/31
500
o
o
500
500
o
500
500
o
o
500
o
500
ACTIVITY (cpm)
In situ plant radioactivities on 1970-15 spoil at Colstrip study area -
replication 3, 1977.
-------
YAMAC SOIL
4/18
4/30
5/12
5/30
6/14
15
SIca 1
Trdu
46
Pasa
7/8
7/19
7/31
E
~ 76
J:
I-
Q.
W
Q
I- 107
'" Z
w
0 :E
'" w Trdu
a:
~ 137
C/)
c(
w
:E
183
214
o
500
500
o
500
o
500
o
o
ACTIVITY Icpm)
500
500
500
500
o
o
o
Fig. C-13.
In situ plant radioactivities on Baxwell-2 undisturbed soil at Colstrip study
area in 1977.
-------
4/18 5/1
SlcO-1
15
SlcO-2
46
5/11
5/31
.......
E
~ 76
x:
~
Q. Slco
w
Q
N ~ 107
o Z
~ w
:::IE Slco
w
a:
::::I 137
en
c(
w
:::IE
183
Fig.
214
o
500
o
500
o
500
BUSBY SOIL (81
6/17
o
500 0 500
ACTIVITY (cpm)
C-14.
7/9
7/18
7/31
o
500
500
o
o
500
In situ plant radioactivities on Chinook-8 undisturbed soil at Colstrip study
area in 1977.
-------
N
g
E
~
~
I-
a.
w
Q
I-
Z
w
2
w
a:
:;)
f1)
C
w
2
107
137
183
214
Fig. C-15.
4/18
Grsq 1
15
Popr 1
46
76
o
500
1948 SPOIL
5/1
5/13
5/31
6/15
o
7/9
7/19
7/31
102'
Popr
500
o
500
o
soo
Agtri
Popr - 2
Arlu
Agtr
o
500
500
In situ plant radioactivities on 1948-3 spoil at Co1strip study area in 1977.
500
o
500
o
o
ACTIVITY (cpm)
-"
-------
46
E
u
76
X
I-
Q.
W
0
I-
Z
N W
0 ~
V1 w
a:
::J
en
<
w
~
P Chvis ~ p
pAgel
~Brin
Lase
Chvls
I I I
4/17
4/30
15
107
137
183
214
o
500
o
500
o
1969 SPOIL
5/13
7/31
5/31
6/17
7/10
7/20
500
o
500
o
500
o
500
o
500
o
500
Fig. C-16.
In situ plant radioactivities on 1969-14 spoil at Co1strip sty area in 1977.
ACTIVITY Icpm)
-------
E
E.
76
J:
~
0.
UJ
0
~ 107
N Z
0 UJ
0\ ~
UJ
II:
~ 137
II)
C(
UJ
~
183
214
ChvlS
15
46
o
Fig. C-17.
1972 SPOIL
4'17
4/30
5/13
5/31
7 10
7 20
7/31
617
Agcr
500
o
o
500 0 500
ACTIVITY (cpmJ
In situ plant radioactivities on 1972-13 spoil at Co1strip study area in 1977.
500
500
o
o
500
500
o
o
500
-------
46
E
u
:J: 76
~
Q.
W
0
~ 107
Z
N W
0 :IE
...., w
~
:;)
f/) 137
c(
W
:IE
183
Agcr
15
214
o
Fig. C-18.
4/16
5/14
4/30
Brin-1
500
o
o
500
500
o
1973 SPOIL
5/31
6/17
500
o
7/9
7/20
7/31
Brin
Brin2
Agcr
500
o
500
o
500
Agel
500
o
In situ plant radioactivities on 1973-12 spoil at Co1strip study area in 1977.
ACTIVITY Icpml
-------
46
E
,g
J: 76
t-
~
W
C
N t- 107
o Z
oo w
:E
w
a:
:;,
en 137
C(
W
:E
Fig. C-19.
pMeal 3823 12~6 -, :=J ~
~gda? 1305 11826 5139 1905 I ]
Agda 1
Meal
-
I I ! _! !
416
4/30
15
183
214
o
500
o
500
o
1975 SPOIL
5 11
5/31
617
7120
710
731
500
o
500 0 500
ACTIVITY (cpm)
500
o
500
o
o
500
In situ plant radioactivities on 1975-11 spoil at Co1strip study area in 1977.
-------
Table C-l. Plant activity index (PAl) values obtained from native range
soils near Colstrip, Montana.
----~---------- ----------
Injection 1976 Inj ec t ion 14!;
4/17 h/1,) ; /4 7 /! q 7/'31
(em) 6/27 7/16 8/9 Depth (em) Specics ~ 5/1 5.'11
SHe lJepth Species
282 )06 -245 15 TRDl' 1 11 )) 66 1 ; ~ -" 701 - sn7
CH1~UOK-I 1) STCO
KiJCR 1 ...,:.l! Jc 235 339 4; -72 -10:-
46 STCO 126 "44 -2':'8
9 132 -147 -h'.J ')
76 STCO II STCO 1
25 27 STCO 1 -,7 57 -.'
MIPS
NSPP 2 2H 156 4Jl -1 l)c -h7~
107 KOCR )4 -ll
) STCO 2 14 25 157 22q 67; 48'; 1216
KOCR )
137 NEOF 25 -15 )0 U\~~O 2 I'
51 CO ) 6 J" 11) JOh h] - (,(J -; ':',,"\
ASCI 1"
TRDl' 1 11 1h 109 ](1) -77 -l.?h -100
KOCR 43 '1n 2fd -h1 211
ARFR 1 -...-j ~
181 KOCH 21 H6 ] ~ \ - ',~b )h
STcn 1
CH]N 5 I)') -72 -1 ,
pn~A 1 - .tJ
TRIJU -19 -] 1 -6
46 ARFR I
STCO "7 -211 1961 -706
STCO 1
LF'11) 7(, -)] 100 .~ (I', -510
STCi) 1 K"O 2 I', 168(1 -60)
STCO ~h 171 -11 -192 hh
S'J('() I -12 "" ~ '~ 'I
HI)!,r: - 7 -71 - 2 I
If! TRDl' 1 It, IOB7 -R2
"'Tcn \9 741 .~ I 'I' j ".
KOCR -(jH 11
107 STf(j lOB 238 -1 'Ih
STcn 2 ~ 72 'j Ir)I)!) ] H" 'I
STCO . ] I -2 -]
137
80XIJELL- 2 15 ARLO 152 1"
BRTE 76 )06
TRDU 15 -25
46 BRIE 22 25
POSA 13
ARLO 70
76 ARLO 8
BRIE 5 16 2)
RIEDEL-6 15 STCLJ 194 525 -111
CHVIL
46 PEPU 170 446 "50
CHVIL 1
KOCR 10
POSA 13 -~
76 PEPl' 187 27~
PSAR )1 )04
STCO
)5 ]) ::-.[( n 1 h 53 :'(1 -7(-) ]"
CHINOLJK-8 15 8RJA ] hK 8, - .,rl 2') 1
]) If\'! L trY..:
ARLO I, '," ] 4 2
CALO 15 <-;T(I)
5) 170 ,9(1 "h ~.rcu - . 2f, .. \.I,'j - r~ 1 ~
46 CHI'IL
]9 12 STC!) .cR -] (J J 73
CALO
-) - -,(1 7h STcn ]FHJ Ie, \4 6 1)(1 - 7 IH
76 C]]VIL j()h
AkDk 17 -1 I ]2 I:) I~ '. II)
MIPS H -'.d7
BIJr.f< ]%
1)7 AR[)R
(.,\LO
209
-------
Table C-2. Plant activity index (PAl) values obtained from old mine
soils near Colstrip, Montana.
Injection 1976 Injection 1977
Site Depth (em) Species 6/27 7/16 8/9 Depth (em) Species ~ 4/17 5/1 5/13 6/15 7/9 7/19 7/ Jl
1948-3 15 GRSI 11 200 87 -19 -28 -5 -69
GTRI 15 239 23 -65 -119 -126
GRS2 4 -24 -7 -72
paPR 2 -90 25
46 POPR 4 14 51 180 -]80 38
POPR 84 134 -241 20 -101
AGTR 2 -291 -58
76 ARLU 6 -20 -11 -6
1928- 5 15 ARDR 13 24
46 ARDR 43 182
76 ARDR 1 106 -23
rSAR 6 12
107 ARDR 10 0
1928-7 15 ARCA 69 34
ARDR 70 74
46 ARDR 12 -2 38
f!EOF 22
MIPS 2
76 IIEOF Jl
137 AIIDR 83
STCO
MIPS
1928-9 15 ASCI 9 -5
PEru 29
76 flEOF 123
AMPS 2 11
STCO 1
107 ARDR 66 -6
137 STCO 1 4
ARDR 2 15
1929-10 15 ROWO 20 86 -41 15 ROWO ] 1
46 AGSP 3 20 AGSP 1 12] 62 -2 -123
HEOr 11 26 POPR 1 31 226 252 -195 -303
76 AGSP 20 -8 -4 AGSP 2 4 50 -38 -70
MEOF 3 9 LAPU 2 353 405 -233 -147
107 AGSP 2 LAPU 2 179 36 -260 -65]
IIEOF ARLO 2 3 13 8 -99
LASE ARFR 3 4 12 152 -32 -9 -5
AGDA 19 AGSP ] 8 12 -22 124 -92 -48
137 IIEaF 15 46 AGSP 1 18 -2 4 -] -1 -1
GUSA 2 4
AGSP 2 16 2696-1480 -1138
AGSP 3 15 -3 -1 -1
76 STCO 3 9 26 269
KOLR ] 6 218 56]
210
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Table C-3. Plant activity (PAl) values obtained from new mine
soils near Co1strip, Montana.
INJECTION 1976 INJECTION 1971
SITE DEPTH (cm) SPECIES 6/27 7/16 8/9 DEPTH Ccm} SPECIES REP 4/17 5/1 5/13 6/15 7/9 7/ 1'"1 7IJl
1975-11 15 ACSH 55 -21 15 MEOF 18 599 -370 28 -86 -~)..
46 SAKA 495 ACDA 2 5 -1)2
AVFA 5 -2 ACDA 165 1491 -273 -174 136 -548
76 HEOF 3 -2 -1
197)-12 15 BRJA 4 15 AGCR 13 -1 JJ 3 -25 -lJ
AGCR 13 65 -24 BRIN 2 17 40 " -119
46 AGCR 5 BRIN 10 209 -418
BRJA 46 BRIN 92 221 -118
ACCR 2 -106
76 AGEL 26 -11 -40
1972-13 15 MESA 242 27 209 15 ACCa 6 1 54 -In -0]
ACCR 3 7 MESA 1 27 6 -2\ -lJ
46 MESA 3 14 4 BRIN 11 90 49 -1)0 110
76 MESA 1 10
ACCR 3 4 -4
SRU 1
107 BRIN
137 AGCR
1969-14 15 HEOF 22 3 15 CHV1 3 -21 -11
CHV' 5 -12 AGEL 11 -85 -250;
46 CHV' 7 -7 BRIN 1 -19 -10
BRIN 8 -18 46 LASE 1 -14 -7
76 CHVI 9 107 CHV' 1 38 -15
AGEL 19
107 AGEL 2 -4
CHV' 4
137 AGEL 12
CHVI 7 7
BRJA 13 -31
183 CHVI 3
1970-1) 15 HEOF 'B 0 58 15 BRIN 2 128 15 76 -)8]
ACCR 15 56 9 AGCR 7B 175 1319 25 -226 -545
46 STca 11 8RIN ' 41 -4 -2 -,
KESA 16 161 21 Acca 10 24 '9 -39 -20
AGCR 14 1 BRIN 1 16 41 -50 -26
BRIN 10 6 Ar.lL 2 -1 -11 -2 -1
76 Acca 2 IRIN 11 20 -31 -23
AGEL 10 16 46 AGCR 5 -hh -'):'
HESA 46 33 ACDA 3 -)9 -21
107 Acca 2 137 ACTR 2
AGEL 45 1C3 ACEL 1
137 DOSA
BRlN
183 51CO
AGEL
211
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---, -.-----
TECHNICAL REPORT DATA
(Please read lIu/ructions on the reverse before completing)
1. REPORT NO. 12. 3. RECIPIENT'S ACCESSIOIII'NO.
EPA-600/7-79-l00
4. TITLE AND SUBTITLE 5. REPORT DATE
SOIL GENESIS, HYDROLOGICAL ?ROPERTIES, ROOT April 1979 issuing date
CHARAGTERISTICS AND MICROBIAL ACTIVITY OF 1- TO 50-YEAR 6. PERFORMING ORGANIZATION CODE
OLD STRIPMINE SPOILS
7. AUTHOR(S) W. M. Schafer, G. A. Nielsen, 8. PERFORMING ORGANIZATION REPORT NO.
D. J. Dollhopf, and K. Temple CR-2
9. PERFORMING ORGANIZATION NAME AND ADDRESS 10. PROGRAM ELEMENT NO.
Montana Agricultural Experiment Station lNE623
Reclamation Research Vrogram 11. CONTRACT/GRANT NO.
¥ontana State TTniversity EPA-IAG D6-E762
Rozeman ~ontana 59717 SEA-CR 684-15-4
12. SPONSORING AGENCY NAME AND ADDRESS 13. TYPE OF REPORT AND PERIOD COVERED
Industrial Fnvironmental Research Lab. - Cinn, OH 14'''n", 1 1 n/7r::.. rn F./7A
Office of Research and Development 14. SPONSORING AGENCY CODE
TT. s. Environmental Protection Agency EPA/600/l2
Cincinnati Ohio 45268'
15. SUPPLEMENTARY NOTES
This pro.iect is part of the F~A-planned and coordinated Federal Interagency Energy/
Environment ~&n ~rogram in cooperation with TTSDA. SEA-CR.
16. A8STRACT
~eclamation of coal strip-mined land is a major environmental concern. The
future of reclaimed land depends on the long-term stability of the soil-vegetation
systeM on mined land. "0 evaluate some of the possible changes that occur in mine
soils through time; soil genesis, water flow patterns, root development, and microbial
activity were studied on natural soils and 1- to 50-year-old minesoils.
Similar soil development processes occur in both minesoils and natural soils,
but because mine soils have a different origin, they will probably always remain
djfferent than natural soils. nifferences in water flow patterns on minesoils and
natural soils were attributed to plant community and soil textural differences.
Roots extended to at least 2 m in mined and unmined soils but root distribution and
root growth patterns varied from site to site as a result of differences in plant
communities, soil temperature, and soil water content. Natural levels of micro-
biological activity were approached on most minesoils within three to five years
after reclamation.
17. KEY WORDS AND DOCUMENT ANALYSIS
a. DESCRIPTORS b.IDENTIFIERS/OPEN ENDED TERMS C. COSA TI Field/Group
Soils Surface Mining Soil Genes 2A, 2D, 6M,
Coal ~lants (botany) Root Development 8H, 8M
r.oal Mines Soil r.hemistry Hicrobial
Spoil Minesoils
Hydrology Montana
Extraction
Reclamation
18. DISTRIBUTION STATEMENT 19. SECURITY CLASS (This Report)' 21. NO. OF PAGES
~elease to the ~ublic TTnclassified 232
20. SECURITY CLASS (This page) 22. PRICE
TTnclassified
EPA Form 2220-1 (9-73)
212
* u. S. OOVERN'-ENT PRINTING OFFICE, 1979 - 657-060/5301
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U.S. ENVIRONMENTAL PROTECTION AGENCY
Office of Research and Development
Environmental Research Information Center
Cincinnati, Ohio 45268
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