Analyses of Four Inceptisols of 

Holocene Age, East-Central Alabama

U.S. GEOLOGICAL SURVEY BULLETIN 1589-C

Prepared in Cooperation with the U.S. Department 

of Agriculture, Soil Conservation Service
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Chapter C

Analyses of Four Inceptisols of 

Holocene Age, East-Central Alabama

By H.W. MARKEWICH, W.C. LYNN, M.J. PAVICH, 

R.G. JOHNSON, and J.C. MEETZ

Prepared in Cooperation with the U.S. Department 

of Agriculture, Soil Conservation Service

Detailed analyses of soils developed in Holocene-age 

alluvium of the lowest terrace along Uphapee Creek 

and the Tallapoosa River in east-central Alabama

U.S. GEOLOGICAL SURVEY BULLETIN 1589

PEDOLOGIC STUDIES IN THE EASTERN UNITED STATES: RELATIONS TO GEOLOGY
DEPARTMENT OF THE INTERIOR 

DONALD PAUL MODEL, Secretary

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director

Any use of trade names and trade marks 

in this publication is for descriptive 

purposes only and does not constitute 

endorsement by the U.S. Geological Survey

UNITED STATES GOVERNMENT PRINTING OFFICE : 1988

For sale by the

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Library of Congress Cataloging in Publication Data

Analyses of four inceptisols of Holocene age, east-central Alabama.

(Pedologic studies in the eastern United States, relations to geology; ch. C) (U.S. 

Geological Survey bulletin ; 1589-C)

Bibliography: p.

"Prepared in cooperation with the U.S. Department of Agriculture, Soil 

Conservation Service."

Supt. of Docs, no.: I 19.3:1589-C

1. Inceptisols Alabama Composition. 2. Soils Alabama Composition. 3. 

Soil formation Alabama. 4. Alluvium Alabama. 5. Geology, Stratigraphic Holocene. 6. Geology Alabama. I. Markewich, Helaine W. 

II. United States. Soil Conservation Service. III. Series. IV. Series: U.S. 

Geological Survey bulletin ; 1589-C.

QE75.B9 no. 1589-C 557.3 s [631.4] 88-600330

[S599.A4]
PREFACE

Some geologic investigations of Quaternary deposits, especially in the conterminous United States, have attempted to use relative degrees of weathering and soil 

formation to establish chronosequences of glacial and (or) fluvial landforms. Most 

studies have been in the glacial terrane of the midcontinent and the Western United 

States. Few such studies have been conducted in the Eastern United States, especially in 

the unglaciated Middle Atlantic and Southeastern States.

From 1979 to 1984, the U.S. Geological Survey and the U.S. Department of 

Agriculture's Soil Conservation Service conducted cooperative regional studies of the 

relations between soils and geology in the Middle Atlantic and Southeastern States. 

The primary goal of the studies was to determine if soil properties could be used to 

estimate ages of associated landforms. Coral, wood fragments, and peat were sampled 

from constructional landforms of fluvial and marine origin in order to estimate ages by 

isotopic analyses; these ages were then related to regional biostratigraphic and 

lithostratigraphic correlations. Specific site investigations were conducted on Pliocene 

to Holocene marine and fluvial terraces in the Atlantic and eastern Gulf Coastal Plains 

and the Appalachian Piedmont. Soils on granite, schist, and quartzite parent rocks of 

the Appalachian Piedmont were sampled to test the use of soil properties as indicators 

of soil age. Each chapter of this bulletin series examines the relation of soils to geology 

in a specific geographic area.

The cooperative study involved research scientists from both agencies and field 

personnel from State offices of the Soil Conservation Service. Responsibility for 

sample analysis was divided between the Department of Agricultures's National Soil 

Survey Laboratory in Lincoln, Nebr., and the U.S. Geological Survey in Reston, Va. 

This report was prepared by scientists from both agencies who participated in specific 

site investigations or in studies of pedogenic processes.

Preface III

CONTENTS

Preface III

Abstract Cl 

Introduction Cl

Classification of soils Cl 

Geologic setting C3 

Field and laboratory methods C4 

Acknowledgments C4 

Results C4

Data presentation C4 

Physical properties C4

Depositional characteristics of alluvium C4 

Effects of pedogenic processes C6 

Mineralogy C6

Optical mineralogy of very fine sand fraction C6 

Mineralogy of the clay-sized fraction C6 

Chemical properties C8

Effects of parent material composition and geographic position 

Bulk chemical analyses C9 

Discussion C9

Clay mineralogy C9

Alteration of clay mineralogy by chemical processes CIO 

Stratigraphy versus pedogenesis C12 

Conclusions C13 

References cited C13 

Tables 1-7 C15

C8

FIGURES

3. 

4-7.

TABLES

Map showing location of study areas and study sites along Uphapee 

Creek and the Tallapoosa River in east-central Alabama C2 

Schematic diagram of the stratigraphic relations between terrace 

alluvium, a lens of carbonaceous clay and sand and leaf material, and 

the underlying sands and clays of the Cretaceous Tuscaloosa Group C4 

Plot of the percentages of <2-//m traction of the four study pedons C5 

X-ray diffraction patterns for:

4. PedonS81AL-087-001 C7

5. PedonS81AL-087-002 C7

6. Pedon S81AL-101-001 C8

7. PedonSSlAL-101-002 C9 

Graphs showing weight percentages of:

A. Fe 2O3 , A1-,O3 , and SiO2 plotted by depth for each horizon of

each pedon CIO

B. SiO2 and zircon plotted against depth for each horizon of 

each pedon Cll

Analytical methods and units of expression for analyses conducted at 

Soil Conservation Service National Soil Laboratory C16 

Pedon S81AL-087-001:

A. Field description C17

B. Textural analysis C17

C. Physical and chemical analyses CIS

D. Optical mineralogy of very fine sand fraction of 

selected horizons C19

E. Bulk chemistry C19

Contents V
3. PedonS81AL-087-002:

A. Field description C20

B. Textural analysis C20

C. Physical and chemical analyses C21

D. Optical mineralogy of very fine sand fraction of

selected horizons C22 

E. Bulk chemistry C22

4. PedonS81AL-101-001:

A. Field description C23

B. Textural analysis C23

C. Physical and chemical analyses C24

D. Optical mineralogy of very fine sand fraction of

selected horizons C25 

E. Bulk chemistry C25

5. PedonS81AL-101-002:

A. Field description C26

B. Textural analysis C26

C. Physical and chemical analyses C27

D. Optical mineralogy of very fine sand fraction of

selected horizons C28 

E. Bulk chemistry C28

6. Intervals of maximum clay accumulation versus intervals of translocated 

clay C29

7. Particle-size distribution of sand on a clay-free base for each pedon C29

VI Contents
PEDOLOGIC STUDIES IN THE EASTERN UNITED STATES: RELATIONS TO GEOLOGY

Analyses of Four Inceptisols of Holocene 

Age, East-Central Alabama

By H.W. Markewich, 1 W.C. Lynn,2 M.J. Pavich ;

Abstract

Four soils developing in terrace alluvium of Uphapee 

Creek and the Tallapoosa River in east-central Alabama were 

described, sampled, and analyzed. The 14C ages of the 

alluvium are between 5,000 and 7,500 years. Field classifications of the four pedons ranged from Dystrochrepts to 

Hapludults, but textural, mineralogical, and chemical analyses 

indicate that all four pedons should be classified as Fluventic 

Dystrochrepts. Data indicate that there has been minimal 

chemical and (or) mineralogical alteration of the alluvium. 

All of the pedons have significant clay content, but only two 

pedons show evidence for clay movement and in situ 

alteration of clay minerals. The best evidence for clay films is 

found in one of the two pedons that do not have argillic 

horizons. Different interpretations of field and laboratory 

data raise questions about textural classification of argillic 

horizons.

Soils developed in the terrace alluvium of Uphapee 

Creek are more smectitic than those developed in the 

alluvium of the Tallapoosa River terraces. All the soils are 

predominantly kaolinitic. Differences in clay mineralogy 

reflect differences in provenance between the two drainage 

basins.

The low pH and high aluminum saturation values for 

the two pedons developed in Uphapee Creek alluvium 

appear to be directly related to (1) the lignitic and pyritiferous 

composition of the Cretaceous sands and clays into which the 

channel of Uphapee Creek is cut, (2) the shallow subsurface 

flow of water from the Cretaceous sediment into the terrace 

alluvium,and (3) the frequent flooding of the terraces caused 

by the infiltration of flood water through the alluvium.

INTRODUCTION

Data obtained from investigations into the rates of 

soil formation are the foundation of soil chronosequence 

studies. Determining the rates of the chemical reactions 

and physical alterations involved in soil formation 

(pedogenesis) is necessary before absolute ages, based on 

the degree of development, can be assigned to individual 

soils. It has been suggested that the rates of chemical and

'U.S. Geological Survey, Doraville, GA 30360.

U.S. Department of Agriculture, Soil Conservation Service, 

National Soil Survey Laboratory, Lincoln, NE 68508-3866.

3 U.S. Geological Survey, Reston, VA 22092.

U.S. Department of Agriculture, Soil Conservation Service, 

Auburn, AL 36830.

3 R.G.Johnson, 3 and J.C. Meetz4

physical soil-forming processes decrease, or become 

asymptotic, through time (Nikiforoff, 1949; Birkeland, 

1984). Although some studies have suggested that this 

hypothesis is not completely correct, there appears to be 

agreement that initial weathering and soil-forming rates 

are rapid and decrease through time (Birkeland, 1984). 

This report presents data from detailed chemical and 

physical analyses of Holocene age soils developed on 

terraces of Uphapee Creek and the Tallapoosa River in 

east-central Alabama. The data show that, for soils 

developed in 5,000- to 7,500-year-old alluvium in eastcentral Alabama, many of the chemical processes involved 

in weathering are related to the physical environment of 

the terrace and to the mineralogy of the parent material. 

Although these chemical processes have little effect on 

horizonization, they do influence cation exchange capacity 

and base saturation of the soils. Some physical characteristics of soils, such as clay films, can persist through 

erosion and subsequent redeposition to become indigenous 

short-term characteristics of the new parent material. (This 

phenomenon is particularly common in overbank deposits.) 

Textural characteristics of the parent material, such as 

fining-upward depositional sequences, are dominant over 

the pedogenic textural characteristics (horizonization) of 

the soil .

Classification of Soils

Many of the soils developing in the Piedmont and 

Coastal Plain of Alabama are in the Ultisol soil order (Soil 

Survey Staff, 1975). Ultisols are found in middle to low 

latitudes in areas where, in some seasons, precipitation is 

greater than evapotranspiration. Water is thus allowed to 

move through the solum into the underlying parent 

material. In Ultisols, leaching removes bases from sola at 

the same rate or at a rate more rapid than that at which 

bases are released from sola by weathering. Most bases are 

held in surface vegetation and in the upper few centimeters 

of sola. Common clay minerals include kaolinite and 

hydroxyinterlayered vermiculite. Halloysite and gibbsite 

are also present in small amounts. Clay-sized quartz, 

goethite, hematite, and muscovite are common. Argillic 

horizons of Ultisols commonly have base saturation values 

(by sum of the cations) of less than 35 percent.

Inceptisols are present on flood plains and on the 

lowermost terraces of many Coastal Plain drainages and

Analyses of Four Holocene Inceptisols in Alabama C1
85°30'

32°30'

32°15'

MOMT<jrjMEriv COUNTY

Base by U.S. Geological Survey 

State of Alabama, 1:500,000 10 20 MILES

10 20 

EXPLANATION

T

30 KILOMETERS

Eutaw Formation "f <*- } Tuscaloosa Group Piedmont rocks

Figure 1. Location of study areas and study sites along Uphapee Creek and the Tallapoosa River in east-central Alabama. 

Patterns designate the main geologic units of the region. Map scales are given for the detailed maps of each study area.

C2 Pedologic Studies in the Eastern United States
are commonly associated with the Udult suborder of 

Ultisols (Soil Survey Staff, 1975). The base saturation 

values of Inceptisols are generally greater than those of 

Ultisols. Their percentage of weatherable (labile) minerals 

may be greater, and (or) their horizonization may be less 

well developed. Clay mineralogy is generally similar in the 

two soil types.

On the basis of field descriptions, two of the soils 

described in this study were assigned to the Udult suborder 

of Ultisols, and two soils were assigned to the Dystrochrept 

suborder of Inceptisols. Each soil described has physical 

characteristics attributable to both parent material and 

pedogenic processes. Reevaluation of the field data, in 

combination with microfabric studies and laboratory 

analyses, indicates that all four soils should be classified as 

Fluventic Dystrochrepts.

Geologic Setting

The Tallapoosa River drains the Coastal Plain of 

Alabama and the Piedmont of Alabama and Georgia. 

Uphapee Creek, a major tributary of the Tallapoosa, joins 

the river in the upper Coastal Plain of east-central 

Alabama 25 km south of the boundary between the 

Piedmont and the Coastal Plain (fig. 1). Like the 

Tallapoosa River, Uphapee Creek drains both Piedmont 

and Coastal Plain terranes, but Uphapee Creek is predominantly a Coastal Plain drainage, incised into the nonmarine 

Upper Cretaceous Tuscaloosa Group (Markewich and 

Christopher, 1982b). Palynological data indicate a 

Tuscaloosa age (early Late Cretaceous) for the sediments 

exposed in the channel of Uphapee Creek east of Chehaw, 

Ala. The sediments are characterized by petrified and 

lignitic wood fragments, which are commonly associated 

with crystalline pyrite. Uphapee Creek west of Chehaw 

and the Tallapoosa River downstream of its junction with 

Uphapee Creek are incised into a stratigraphically younger 

sandy unit 30 m thick that was mapped as part of the 

Tuscaloosa Group by Markewich and Christopher (1982b). 

No palynological data were available for these strata, 

which only locally contain small amounts of pyrite-rich 

lignitic material. Marine sands and clays of the Upper 

Cretaceous Eutaw Formation (Markewich and Christopher, 1982b) stratigraphically overlie strata of the 

Tuscaloosa Group, crop out along the northward flowing 

tributaries of Uphapee Creek and the Tallapoosa River, 

and cap the interstream divides south of these two streams

(fig- I)-

The four pedons sampled for this study are from the 

terrace directly adjacent to Uphapee Creek and the 

Tallapoosa River (fig. 1). This terrace, the dominant 

geomorphic feature of both valleys, is continuous for 64 

km. The degree of modification of the terrace surface 

increases downstream, and radiocarbon ages from wood at 

the base of the alluvium suggest the possibility of two

depositional periods. The 14C ages of 5,260±90 and 

5,470+100 yr B.P. for the terrace at sites 3 and 4 

(Markewich and Christopher, 1982a) appear to be from a 

part of the terrace that has been extensively modified by 

flooding, or else they represent the age of a terrace that is 

inset into the main terrace. The main terrace has radiocarbon ages of 6,360+110 and 7,520+110 yr B.P. 

(Markewich and Christopher, 1982a). Because it is difficult 

to geomorphically separate the two surfaces and because 

the difference between the maximum age of the younger 

surface and the minimum age of the older is less than 1,000 

years, the two surfaces are considered as one terrace for 

this report. 5

Alluvium associated with the main terrace is dominantly a fining-upward sequence of pebble- to cobblesized gravel to medium- to fine-grained sand and silt. The 

sand- to cobble- sized fraction of the alluvium is dominantly 

quartz and contains a small percentage of rock fragments. 

The silt fraction is predominantly quartz. The terrace 

alluvium varies in thickness from 2 to 7 m and commonly 

has an abrupt lower contact with the underlying sediments 

of Cretaceous age. At each locality, the dated material was 

collected from carbonaceous lenses near the alluviumCretaceous contact. A diagrammatic sketch in figure 2 

shows the relation between the terrace alluvium, a lens of 

carbonaceous clay and leaf material, and the Cretaceous 

sands and clays near site 2. The stratigraphic relations 

presented in figure 2 are representative of the relations at 

each of the sample localities.

Locally, younger sediments are cut into the main 

terrace. Wood from meander-bend deposits that cut into 

the terrace near site 1 yielded a 14C age of 250+70 yr B.P. 

Clay balls in alluvium of the main terrace near site 1 

contain fragments of wood of Pleistocene age; one fragment, tentatively identified as jumper, yielded a I4C age of 

27,000+520 yr B.P. (Markewich and Christopher, 1982a).

Both the microfossil and macrofossil data indicate 

that Holocene deposition has been under humid subtropical 

climatic conditions similar to those found in the area today 

(Shipp, 1985). The flora has been dominated by pine and

Specific definitions of the terms "flood plain" and "terrace" vary 

with the perspective of the user (for example, geomorphologist, pedologist, 

or engineer) and with the objective of the study. Linsleyand others (1975, 

p. 428) defined the flood plain of a river as "the valley floor adjacent to the 

incised channel, which may be inundated during high water." The term 

"terrace" has generally been used to mean an aggradational form, or a 

thin accumulation of unconsolidated material on a beveled surface, 

contained within a valley and composed of unconsolidated material that 

is found along the border and above a stream or river. A terrace is 

generally considered to mark a former water level or flood plain. Both 

Uphapee Creek and the Tallapoosa River periodically fill their respective 

channels and flood onto their flood plains and (or) the adjacent terrace. 

Flood intervals can be as often as twice a year or as infrequent as once in 5 

years. Thin layers of silty sand, present as irregular patches on those parts 

of the terrace within several tens of meters of the stream channels, appear 

to be the result of periodic floods, but flooding causes no other apparent 

modification to the surface morphology of the terrace.

Analyses of Four Holocene Inceptisols in Alabama C3
Figure 2. Stratigraphic relations between terrace alluvium 

(a fining-upward sequence), a lens of carbonaceous clay 

and sand and leaf material, and the underlying sands and 

clays of the Cretaceous Tuscaloosa Group (bottom unit).

oak forest, along with shrubs, herbs, and aquatic plants 

(Markewich and Christopher, 1982a; Shipp, 1985).

Field and Laboratory Methods

For the purpose of this report, the pedons sampled 

are considered to be developed in alluvium of the lowest 

terrace; all sites are within 26 m laterally of the stream 

channel. The level of water in the stream channel controls 

in part the water table in terrace alluvium and influences 

the agricultural use of the terrace.

The four study pedons were described and sampled 

by the authors and local personnel from the U.S. Department of Agriculture's Soil Conservation Service (SCS). 

Pedon numbers are standard SCS notation, which gives 

the year, the State abbreviation, the county number, and 

the pedon number in the county (for example, S81AL-087- 

001). Pedons discussed in this report are referred to by the 

last six digits of their complete pedon numbers. Horizon 

designations follow the revision of the Soil Survey Manual 

(Soil Survey Staff, 1981) and also a brochure produced by 

Cornell University and the Department of Agriculture's 

Agency for International Development (Soil Survey Staff, 

1986). New horizon designations are used in the text of this 

report; both old and new designations are given in the 

illustrations and tables. Samples were sent to the SCS 

National Soil Survey Laboratory (NSSL) in Lincoln, 

Nebr., where they were split; one set was then sent to the 

U.S. Geological Survey (USGS) laboratories in Reston, 

Va., and the other was retained by the NSSL. Samples 

were analyzed for standard physical and chemical characteristics at the NSSL. Some of the analyses conducted at 

the NSSL are particle-size distribution, cation exchange

capacity, pH, base saturation, and X-ray diffraction on the 

<2-/um fraction of selected horizons (magnesium saturated 

at room temperature, magnesium saturated and glycerol 

solvated at room temperature, potassium saturated at 300 

and 500° C). Diffraction patterns presented in this report 

represent glass-mounted slides of clay that were magnesium 

saturated at room temperature. The USGS laboratories 

conducted additional analyses, including bulk chemistry 

by X-ray fluorescence and analyses of iron and aluminum 

by oxalate extraction and by atomic absorption.

Acknowledgments

We would like to express our appreciation to J.P. 

Owens, R.B. Mixon, and J.T. Hack of the U.S. Geological 

Survey and R.B. Daniels and Klaus Flach of the Soil 

Conservation Service for their initiative in suggesting a 

cooperative project between the two agencies and for their 

encouragement throughout the study period. We also 

extend our thanks for the assistance of Soil Conservation 

Service field personnel in sampling the study profiles. Cleo 

Stubbs, Wade Hurt, H.R. Finney, and James Brown 

helped to select the field sites and describe the pedons.

RESULTS

Data Presentation

Exact descriptions of the soil and weathering profiles 

at each site are given in tables 2A 3A, 4A, and 5^4. 

Analytical results for samples from the profiles are 

presented in tables 2B-E, 3B-E, 4B-E, and 5B-E. Table 6 

shows evidence for translocation of clay by pedogenic 

processes as opposed to depositional clay for each profile, 

and table 7 presents particle-size distribution data on a 

clay-free basis. Site 1 is the farthest upstream along 

Uphapee Creek. Site 4 is located approximately 48 km 

downstream from the junction of Uphapee Creek and the 

Tallapoosa River (see fig. 1). Figure 3 is a graphic 

presentation of the study pedons that shows the weight 

percentage of the <2-^m fraction for each profile, plotted 

by horizon. X-ray diffraction patterns of the <2-/um 

fraction are presented in figures 4 through 7. Figure 8^4 

shows variation with depth of Fe2O3, A12O3, and SiO2 by 

weight percent. Figure SB shows variations with depth of 

zircon (in parts per million) in comparison with the weight 

percentage of SiO2.

Physical Properties

Depositional Characteristics of Alluvium

Textural data from all four pedons show that the 

soils are developing in fining-upward sequences of fluvial 

sands, silts, and clays. The original stratification is domiC4 Pedologic Studies in the Eastern United States
50

100

150

200

S81AL-087-001

PERCENT <2^m

10 20 30 10

S81AL-087-002 

PERCENT <2fJLm

20 30 40 50

Ap (Ap) 

**"! B21 (Bw1)

B22 (Bw2)

B23t (Bw3)

B24 (Bw4)

::M ,:j BS (BO

IIC1 (C1)

IIC2 (C2)

50

100

150

200" 

A1 (A) 

A2(E)

B21t (Bw)

B22tg (Bwgl)

B23tg (Bwg2) 

B23tg (BtgD

B24tg (Btg2)

10

S81AL-101-001

PERCENT <2fJLm

20 30 40 50

50

100

-- 150

200

250 LB21t (Bw)

B21t(Bt1)

B22t(Bt2)

S81AL-101-002

PERCENT <2fJLm

10 20 30

B23t(Bt3) 

B23t(Bt3)

B3(BC)

HC (C2)

50

inn IUU

- 150

200

250 "-

-AJLJAL

40 

1 

B1 (Bwl)

B21 (Bw2)

B22 (Bw3)

B23(Bw4)

B3(BC)

C(C)

Figure 3. Weight percentages of <2-//m fraction of the four study pedons. Percentages given for composite samples from each 

horizon.

nant over pedogenic horizonization. Data in table IB show 

a threefold increase in the percentage of very fine sand 

toward the surface of pedon 087-001 and a correlative 

decrease in the coarser sand-sized fractions toward the 

surface. Data from pedon 087-002 (table 3E) show a 

decrease in the percentage of sand between 176 and 58 

cm and an increase in silt-sized material above 176 cm. 

Coarser size fractions show variable patterns of distribution. The percentages of very fine and fine sand in pedons 

101-001 and 101-002 (tables 4fi, 5B) are variable with 

depth and appear to reflect variations in fluvial deposition; 

that is, particle- size data support stratification changes at 

22,89,161, and 190 cm at site 4 in pedon 101-001 (tables 6, 

7). The percentage of silt in the upper 2 m (30-50 percent) is

much higher in terrace alluvium from pedons 101-001 and 

101-002 (tables 4B, 5B) along the Tallapoosa River than it 

is in terrace alluvium from Uphapee Creek (4-35 percent) 

(see tables 2B, 3B). The percentage of clay varies from 1.2 

to 50 percent. Clay maxima do not appear to be coincident 

with maxima of pedogenic development. In both pedons 

101-001 and 101-002, clay maxima are reached within 30 

cm of the surface, and the percentage of clay decreases 

downward from the clay maxima (fig. 3, tables 4B, 5B).

Preliminary horizon designations of pedon 087-001 

placed a lithologic discontinuity at 73 cm (the top of the 

Bw3 horizon), where there is a significant change in the 

relative percentages of sand, silt, and clay (table 2B). We 

decided to omit the designations of lithologic change, since

Analyses of Four Holocene Inceptisols in Alabama C5
change in particle-size distribution is an indigenous 

characteristic of most alluvial sequences and does not 

imply a change in source material.

Effects of Pedogenic Processes

Pedons at sites 1 and 2 (087-001 and 087-002, 

respectively) show little to no evidence of clay movement. 

Pedon 087-001 has no clay films in any horizon and only a 

weak suggestion of clay bridging in the Bw4 horizon. 

Increases in clay at 26 and 73 cm are sufficient for argillic 

horizon designation, but these depths coincide with evidence for change in the particle size of the parent material 

(tables 2B, 6,7). Pedon 087-002 has clay increases sufficient 

for argillic horizon designation at 36 and 58 cm (table 3E), 

but these increases appear to be related to deposition 

rather than to pedogenic processes. In the Bw horizon, 

there are clay linings in some pores. The linings do not 

completely mask the sand and silt grains. A few reddish 

films on ped surfaces in the same horizon are also present 

in lower Bwg horizons of the same pedon.

Field designations suggested that pedon 101-001 at 

site 3 has a large enough clay increase at 22 cm for argillic 

designation (table 4B). The microfabric of pedon 101-001 

suggests that the first evidence of moved clay is only in the 

lower part of the Bw horizons, beginning at 47 cm. This 

pedon has thin reddish coatings on few faces and oriented 

clay in pores in all Bt horizons. The Bt3 horizon has some 

reddish and black films on ped faces. The black films are 

described as mottles in the pedon description (see table 

4A). Pedon 101-002 has the strongest expression of moved 

clay of the four pedons. This fact is particularly interesting, 

since pedon 101-002 is classified as a Dystrochrept, and an 

argillic horizon was not described. Clay increase from the 

A horizon to the Bw horizon at 8 cm is sufficient for argillic 

designation, but there is also evidence for a change in the 

particle-size distribution of the parent material at this 

depth (tables 6, 7). Although no clay films were described, 

MnO2 cutans were prominent from Bw2 downward. 

Muscovite was evident throughout both pedons 101-001 

and 101-002, but the total content was considered to be 

small (tables 4£>, 5£>).

Pedon 101-002 has unusual distinct strong brown 

clay coatings (7.SYR 5/6, dry) in the A horizon, which are 

unlike those found deeper in the pedon. These clay films 

are probably inherited from a soil that was eroded and 

redeposited as overbank sediments at this locality. This 

hypothesis raises the distinct possibility of intact alluvial 

transport of argillic fabric.

Mineralogy

Optical Mineralogy of the Very Fine Sand Fraction

The very fine sand fraction in each study pedon is 

>70 percent quartz. Potassium feldspar is the dominant

weatherable mineral in these soils (tables 2D, 3Z), 4D, 5D). 

The percentage of potassium feldspar does not change 

significantly between the C and B horizons in any pedon. 

Pedons 087-001 and 087-002 in the Uphapee Creek 

drainage have less muscovite and higher potassium feldspar 

than do pedons 101-001 and 101-002 along the Tallapoosa 

River. The lack of difference in mineralogy between 

horizons in any one pedon suggests that the mineralogical 

differences are related to differences in parent material, 

possibly to differences in provenance between the Uphapee 

and Tallapoosa drainages. For further study, scanning 

electron microscope photographs and photomicrographs 

could be useful to show any surface alteration of feldspar 

grains

Mineralogy of the Clay-Sized Fraction

Pedon 087-001 contains roughly equal amounts of 

smectite and kaolinite, secondary amounts of quartz and 

muscovite, and a trace of gibbsite (fig. 4). This pedon is the 

most smectitic of the four profiles. The C2 horizon 

contains as much smectite as the superjacent horizons, an 

indication that the smectite is in the parent material. The 

broad 15-A peak from the magnesium-saturated sample 

expands to 17 A on glycerol solvation, and a small 10-A 

peak remains. Heating of a potassium-saturated sample to 

350 ° C causes collapse to 10 A of most of the smectite. The 

Bw3 horizon contains a higher percentage of kaolinite and 

vermiculite relative to smectite than the C2 horizon does. 

The kaolinite peaks are sharp, suggesting well- crystallized 

kaolinite. The Bwl horizon contains about the same 

percentages of smectite, kaolinite, and vermiculite as the 

Bw3 horizon. The presence of a high percentage of smectite 

in an acidic soil pH(H2O 4.5 to 4.7, pH(KCl) 3.4 to 

3.9 suggests that the smectite is inherited and that there 

has been insufficient time for alteration. The upward 

increase in kaolinite and vermiculite (presumably aluminum 

hydroxyinterlayered) relative to smectite suggests some in 

situ alteration of smectite.

Pedon 087-002 contains much more kaolinite and 

muscovite relative to smectite than pedon 087-001 does. 

The C horizon of pedon 087-002 is kaolinitic (fig. 5). There 

is a strong smectite peak and a moderately strong muscovite 

peak in horizon C. The Bwgl horizon is also kaolinitic. 

The percentage of smectite in the Bwgl horizon decreases 

relative to kaolinite and mica in comparison with that of 

the C horizon. This decrease may be due to mineral 

alteration and (or) clay translocation. The 14-A nonexpandable vermiculite peak is present, as the glycolated 

sample shows, but its percentage cannot be determined.

In pedon 101-001, the C horizon is predominantly 

kaolinitic and contains secondary amounts of vermiculite, 

smectite, and muscovite (fig. 6). Glycerol solvation of a 

magnesium-saturated sample reduces the intensity of the 

14-A peak and thus indicates a randomly interstratified 

mixed layer assemblage of 2:1 layers. In the Bt3 horizon,

C6 Pedologic Studies in the Eastern United States
S81AL-087-001

138

S81AL-087-002

354

170

7 1

170

138

B21 (Bwl)

B23t (Bw3) B22tg(Bwg1)

IIC (C2)

s s 170

EXPLANATION

K Kaolinite Q Quartz 

S Smectite Untreated 

M Muscovite ---------- Mg saturated,

G Gibbsite glycol solvated

Figure 4. X-ray diffraction patterns of magnesium-saturated 

and glycerol-solvated (magnesium saturated) <2-(jrr\ samples 

from pedon S81AL-087-001. Kaolinite and smectite are 

dominant. Glycerol solvation causes a shift of the smectite to 

a 17-A D-spacing. Gibbsite, quartz, and muscovite are also 

present in small amounts.

Figure 5. X-ray diffraction patterns of magnesium-saturated 

and glycerol-solvated (magnesium saturated) <2-/um samples 

from pedon S81AL-087-002. Kaolinite and smectite are 

dominant. Glycerol solvation causes a shift of the smectite to 

a 17-A D-spacing. Muscovite and quartz are present in small 

amounts.

138

333

IIC(C2)

M K K M,Q 

EXPLANATION

K Kaolinite Untreated 

S Smectite ' -- - Mg saturated, 

M Muscovite glycol solvated 

Q Quartz

Analyses of Four Holocene Inceptisols in Alabama C7
S81AL-101-001

354

B21t(Bt1)

B22t (Bt2)

B23t (Bt3)

IIC(C2)

M,Q

EXPLANATION

V Vermiculite Untreated 

M Muscovite ......... Mg saturated,

K Kaolinite glycol solvated 

Q Quartz

Figure 6. X-ray diffraction patterns of magnesium-saturated 

and glycerol-solvated (magnesium saturated) <2-fjm samples 

from pedon S81AL-101-001. Kaoliniteisdominantthroughout 

the profile. Vermiculite, muscovite, and quartz are present in 

small amounts. In the untreated pattern forthe Bt1 horizon,a 

distinct peak occurs at 13.8 A. On glycerol solvation, no 

distinct peak appears at a higher D-spacing. The high 

background between 13.8 and 17 A suggests the presence of a 

small amount of smectite.

the kaolinite is dominant, and the 10- and 14-A peaks are 

more distinct than they are in the C horizon. Both the 10- 

and 14-A peaks remain with glycerol solvation. In the Btl 

and Bt2 horizons, there are slight increases in the 10- to 

14-A region of the mixed layer relative to the same interval 

in the Bt3 horizon, but all phases are less abundant than 

kaolinite.

X-ray diffraction patterns from samples of pedon 

101-002 are presented in figure 7. The pedon is predominantly kaolinitic and contains lesser amounts of 

smectite, vermiculite, and muscovite. There is little change 

in peak intensities between the C horizon and the Bw3 

horizon. The Bw3 does show slightly greater intensity of 

the vermiculite peak.

For all four pedons, differential thermal analysis 

confirms the presence of kaolinite and corroborates the 

interpretation of X-ray diffraction patterns, which indicated 

that kaolinite is dominant at sites 2, 3, and 4 (pedons 

087-002, 101-001, and 101-002).

Chemical Properties

Effects of Parent Material Composition and Geographic 

Position

Chemical data (tables 2C, 3C, 4C, 5Q indicate that 

all pedons contain appreciable organic carbon (>0.2 

percent), have low bases, are acidic, and have aluminum 

extractable by KC1. Sites in Uphapee Creek (pedons 087- 

001 and 087-002) have somewhat lower base saturation 

and more KCl-extractable aluminum and are more acidic 

than sites along the Tallapoosa River (pedons 101-001 and 

101-002). The lowest pH values of pedons 087-001 and 

087-002 are associated with the 60- to 100-percent values 

for aluminum saturation and correspondingly low extractable bases to depths of 2 m (tables 2C, 3C). Extractable 

bases and pH values are significantly higher and aluminum 

saturation values are significantly lower in pedons 101-001 

and 101-002 than they are in pedons 087-001 and 087-002.

Pedons 087-001 and 087-002 are developed in 

Uphapee Creek terrace alluvium, which overlies lignitic 

and pyrite-rich sands and clays of the Upper Cretaceous 

Tuscaloosa Group. The Tuscaloosa Group as mapped by 

Markewich and Christopher (1982b) also forms the valley 

walls of Uphapee Creek. Repeated flooding of alluvium by 

water that has been derived from and (or) has flowed 

through the pyrite-rich parent material greatly affects the 

acidity of the alluvium and the bulk chemistry of the 

sediment. The parent material may also affect the organic 

carbon content of the soils. The pedons exhibit irregular 

decreases in organic carbon with depth and relatively high 

(>0.2 percent) values of organic carbon to depths of 150 

cm or more.

C8 Pedologic Studies in the Eastern United States
S81AL-101-002

7.1

354

B22 (Bw3)

71

354

140

C(C)

V M K M,Q

EXPLANATION

V Vermiculite Untreated 

M Muscovite --------- Mg saturated,

K Kaolinite glycol solvated 

Q Quartz

Figure 7. X-ray diffraction patterns of magnesium-saturated 

and glycerol-solvated (magnesium saturated) <2-yum samples 

from pedon S81AL-101-002 have essentially the same pattern 

as those from pedon 101-001. Kaolinite isdominantthroughout the profile. Vermiculite, muscovite, quartz, and possibly 

smectite are present in small amounts.

Bulk Chemical Analyses

Some results of bulk chemical analyses are plotted in 

figures &A and 85 (data for each pedon are given in tables 

2E, 3E, 4E, 5E). Figure 8,4 shows, for each of the four 

pedons, the weight percentages of SiO2, A12O3, and Fe2O3

for each horizon versus depth. Figure 85 shows the weight 

percentages of SiO2 and Zr (in parts per million) for each 

horizon versus depth. The distribution patterns of the 

major elements show that SiO2 decreases and A12O3 

increases are correlative with the amount of clay in the 

horizon.

In pedon 087-001, the departures from relatively 

constant weight percentages take place in the clay-rich 

Bw3 and Bw4 horizons. Fe2O3 shows little variation in 

comparison with A12O3 and SiO2. In pedon 087-002, the 

high percentage of kaolinite in the Bw and Bt horizons is 

reflected by high A12O3 and low SiO2 percentages below a 

depth of 30 cm. The decrease of A12O3 and the increase of 

SiO2 with depth correspond to the decreasing percentage 

of clay with depth. In pedon 101-001, SiO2 and A12O3 also 

reflect the percentage of clay. The relatively small variation 

of Fe2O3 suggests that clay distribution rather than 

pedogenic removal of SiO2 is responsible for the A12O3 

distribution. The patterns in pedon 101-002 are similar to 

those in pedon 101-001.

Zirconium values (expressed as parts per million) 

have been used as an index of chemical alteration because 

zirconium is one of the least mobile elements during 

weathering (Sudom and Arnaud, 1971; Harden, 1987). 

Zirconium data from the four pedons plotted on figure 85 

show that zirconium is covariant with SiO2. This covariance 

indicates relatively little movement of SiO2 relative to 

zirconium and suggests that chemical alteration of the 

original parent material has been minimal. These data 

agree with the mineralogical data from the four study 

pedons and with the hypothesis of minimal pedogenic 

alteration of the parent material in these sola.

DISCUSSION

Clay Mineralogy

The amount of smectite in Uphapee Creek alluvium 

is significantly greater than that in Tallapoosa River 

alluvium, owing to the difference in the source areas of the 

sediments. Uphapee Creek is receiving fine-grained sediments from the Upper Cretaceous nonmarine Tuscaloosa 

Group and the marine Eutaw Formation. Residual soils on 

the Tuscaloosa Group in adjacent Lee County, studied by 

Karathanasis and Hajek (1983), have a montmorillonite 

mineralogy, as do many of the soils developed on the 

Eutaw Formation. The Tallapoosa drainage, by contrast, 

contains sediments from the more kaolinite-rich regolith 

(saprolite) developed on the crystalline rocks of the 

Piedmont. The difference in source areas accounts for the 

much higher kaolinite content and the lower smectite 

content of soils at sites 3 and 4 (pedons 101-001 and 

101-002).

Analyses of Four Holocene Inceptisols in Alabama C9
S81AL-087-001 S81AL-087-002

50

100

150 HC1

IIC2

200 0 5 10 15 20 25 50 75 

OXIDES, IN WEIGHT PERCENT

S81AL-101-001

50

100

S 150

200

Ap 

B2lt 

B21t 

B22t

B23t 

B23t

B3 

IIC

25 50 75 

OXIDES, IN WEIGHT PERCENT

(Ap) 

(Bw1)

(Bw2) 

(Bw3)

(Bw4) 

(BC)

(CD 

(C2)

100

(Ap) 

(Bw) 

(BtD 

(Bt2)

(Bt3) 

(Bt3) 

(BC)

(C2)

100

B23tg * L

B23tg A ,

B24tg j k

EXPLANATION 

A Fe2 O3 

 AI 2 O3 

o Si02

(A) 

(E)

(Bw) 

(Bwgl)

(Bwg2)

(BtgD 

(Btg2)

(C2)

0 5 10 15 20 25 50 75 

OXIDES, IN WEIGHT PERCENT

S81AL-101-002

100

A1 

B1

B21

B22

B23

B3

C

_

"

-*

-

(

/

C

1

/

>

! I

I 1

j> (

) 1

r

i

i

\

\

1

1

I i

t

(A) 

(Bw1)

(Bw2)

(Bw3)

(Bw4)

(BC)

(C)

0 5 10 15 20 25 50 75 

OXIDES, IN WEIGHT PERCENT

100

Figure 8A Weight percentages of Fe 2O 3, AI 2O3, and SiO2 plotted by depth for each horizon of the four study pedons.

Alteration of Clay Mineralogy by Chemical 

Processes

Neither the X-ray diffraction patterns nor the bulk 

chemical data show much evidence for chemical alteration 

of minerals in the parent material. Overall, the chemical 

analyses from these profiles support the interpretation that 

the percentage of clay determines the bulk chemistry. The

distribution of the clay, generally increasing toward the 

surface, and the clay mineralogy support the interpretation 

that the clay is depositional rather than pedogenic. The 

lack of chemical alteration is reflected in the relative 

constancy of the Fe2O3 values. If SiO2 loss were responsible 

for the A12O3 increases in the Bt horizons, then Fe2O3 

would increase with A12O3 .

The lack of alteration in potassium feldspar and

CIO Pedologic Studies in the Eastern United States
5°

100

150

200

Ap 

B21

B22 

B23t

B24 

B3

IIC1 

IIC2

S81AL-087-001

Si02, IN WEIGHT PERCENT 

50 75 100

S81AL-087-002

Si02 , IN WEIGHT PERCENT 

50 75 100

(Ap) 

(Bw1) 

(Bw2) 

(Bw3)

(Bw4) 

(BC)

(CD 

(C2)

300 400 500 600 700

Zr, ppm

A1 

A2

B21t 

B22t

B23tg

B23tg

B24tg 

IIC

(A) 

(E) 

(Bw) 

(BwgD

(Bwg2)

(BtgD

(Btg2) 

<C2)

200 300 400 500 600 700

Zr, ppm

S81AL-101-001

Si02 , IN WEIGHT PERCENT 

50 75 100

S81AL-101-002

50

a 100

0 B23t

2i 150

Ci

200

200 300 400

Zr, ppm

EXPLANATION 

O SiO2 

 Zr

Si02 , IN WEIGHT PERCENT

50 75 100

A1 

B1

B21

B22

B23

B3

C

<

<

<

"

X* '

1

(

c

x01

\

1 V

\ -I 

1

i i ~

(A) 

(Bw1)

(Bw2)

(Bw3)

(Bw4)

(BC)

(C)

300 400 500 600 700 I___i I i____|

Zr, ppm

Figure 86. SiO2 (in weight percent) and Zr (in parts per million) plotted against depth for each horizon of each study 

pedon.

muscovite, the most abundant "weatherable parent 

minerals," in less than 10,000 years is not surprising, given 

the slow kinetics. The lack of alteration of smectitic clay is, 

however, unexpected. In soils of the Southeastern United 

States and in areas of significant rainfall and volcanic soils, 

smectite may alter in only a few thousand years (Altschuler 

and others, 1963; Karathanasis and Hajek, 1983). X-ray 

diffraction patterns of the < 2-/um fraction show that 

mineral alteration has been slight. The lack of alteration 

may be the result of the young Holocene age(s) of the 

parent material and (or) of chemical conditions that

enhance the stability of the clay phases originally present. 

Smectite stability in low pH pedons may be the result of 

high dissolved silica activities (Karathanasis, 1982). Concentrations of dissolved elements were not measured at 

these localities, so we cannot comment on dissolved 

components. Chemical data, however, indicate that there 

is no substantial loss of SiO2 from these profiles.

As a test of this hypothesis, we can consider the 

amount of clay in each pedon. The total amount of clay 

formed and removed from eluvial horizons should provide 

an assessment of soil development (if eluvial horizons are

Analyses of Four Holocene Inceptisols in Alabama C11
still intact). Factors of time, climate, vegetation, and soil 

drainage are considered constant for each site. Similar 

drainage assumes that the channel incisions that isolated 

the terraces occurred at a similar time at each site. Parent 

material in the Uphapee drainage differs somewhat from 

parent material in the Tallapoosa, as the latter drains the 

Piedmont as well as the Coastal Plain. Differences are 

evidenced by a higher muscovite content in sands of the 

Tallapoosa sediments. For the moment, assume that 

parent-material differences do not materially alter soil 

development in the two watersheds. The following assumptions and computations are then used to assess soil 

(argillic) development: (1) eluvial and illuvial horizons 

have uniform particle-size distributions at time zero; (2) 

the amount of clay accumulated in illuvial horizons over 

time equals the amount of clay currently present in the 

upper eluvial horizon; and (3) illuviated clay is estimated 

by [(clay percentage in upper B horizon -clay percentage 

in A horizon)Xbulk density of horizonXhorizon thickness] 

for each horizon and summed for the illuvial horizons. If 

soil development is similar for all sites, the magnitude of 

these values should be similar for all sites (if assumptions 1 

and 2 are valid).

A sample calculation for pedon 101-001 is as follows: 

(46.6- 14.8)percent clay X 1.43 g/cm3

X22 cm= 1,000 g/cm2 

The results for all four pedons are as follows:

Pedon

087-001 ........

087-002 ........

101-001 ........

10 1-002 ........

Sampled

as1

.........D

......... P

.........H

.........D

Clay, in g/cm2 Illuviated total clay, 

per horizon in g/cm2

748 + 425 + 572 

815 + 750 

1,000 

194

1,745 

1,565 

1,000 

194

'D, Dystrochrept; P, Paleudult; H, Hapludult.

The results indicate widely divergent values for the 

four sites, and the quantities do not correspond with the 

degree of development suggested by the "Sampled as" 

classification. In summary, these calculations suggest that 

the clay increases from the A horizons to the B horizons are 

not associated with soil development or that there has not 

been enough time for pedogenic processes to alter the 

orginal sediment distribution.

Stratigraphy versus Pedogenesis

To assess soil development, scientists must decide to 

what degree pedogenic processes have made an imprint on 

the soil parent material. In fluvial settings, the parent 

material is characterized by particle-size distribution, 

stratification, mineralogy, and chemistry of the sediment.

Pedogenic development is evidenced by accumulation of 

organic matter that decreases downward from the surface, 

accumulation of clay in a subsurface (argillic) horizon, 

development of soil structure and (or) the obliteration of 

sedimentary structures, and changes in mineralogy or 

chemistry.

Sedimentary structure is obliterated by bioturbation, 

by shrink-swell activity if clay content is high enough, and 

by oxidation of detrital organic components. An argillic 

horizon is evidenced by subsurface accumulation of illuviated clay relative to the overlying horizons. Clay 

accumulates in an argillic horizon by alteration of material 

in place, by original deposition, and by illuviation of clay 

from the overlying horizons. Clay illuviation is evidenced 

by the presence of oriented clay cutans in pores and on soil 

structural (ped) surfaces. Observed illuvial clay cutans are 

noted by a "t" in a horizon designation. Strictly, the "t" 

indicates evidence of moved and deposited clay and is not 

sufficient in itself to identify an argillic horizon. Conversely, 

argillic horizons can and do develop without showing 

evidence of moved clay (Nettleton and others, 1969). Lack 

of oriented clay in upper B horizons may be because of 

degradation or because conditions were never right for 

deposition. If soil structural surfaces are unstable because 

of shrink-swell, clay cutans are destroyed.

In the fluvial setting of the present study, it is 

reasonable to assume that deposits are alluvium and have 

been emplaced no longer than 5,500 to 7,500 years, in 

accord with radiocarbon ages. Sediments within the soil 

profile could be younger if more than one episode of 

deposition postdates the dated carbonaceous material. 

Evidence of stratification (particle-size distribution among 

horizons) is distinct in pedons 087-001 (three episodes), 

101-001 (three episodes, including overbank sedimentation), and 101-002 (three episodes, including overbank sedimentation) and is subtle in pedon 087-002 if it is 

present at all. Evidence of stratification can be assessed by 

computing the particle-size separates on a clay-free base as 

presented in table 7.

Determining the degree of soil development is 

confounded when depositional strata show an increase in 

clay within the depth interval commonly associated with 

the development of an argillic horizon. Table 6 presents a 

summary of the intervals of clay maxima and contrasts 

those with intervals in which microscopic clay cutans are 

observed petrographically. There are significant increases 

in clay percentages at the tops of fining-upward sequences 

in each pedon. For example, in pedons 087-001, there is a 

12- to 27-percent clay increase at 73 cm; in pedon 087-002, 

there is a 7- to 36-percent clay increase at 36 cm; in pedon 

101-001, there is a 14- to 47-percent clay increase at 22 cm; 

and, in pedon 101-002, there is a 21- to 38-percent clay 

increase at 8 cm. These intervals do not correspond to the

C12 Pedologic Studies in the Eastern United States
intervals of petrographically identified clay cutans. The 

evidence for stratification in all these pedons suggests that 

the relative amounts of clay in their upper horizons result 

from deposition rather than pedogenic processes.

CONCLUSIONS

1. Evidence indicates minimal soil development and 

suggests that differences in clay content relate to 

stratigraphy and that there has been no significant 

alteration related to in situ formation of clay minerals.

2. There are differences in the mineralogies of sediments 

in the two river systems and associated differences in 

the chemistries of the sediments. However, these 

differences have had no measurable effect on soil 

development. Differences in chemical properties are 

related to differences in source sediments rather than 

to differences in soil development.

3. Data indicate that, even under the humid temperate to 

humid subtropical environment of the upper Coastal 

Plain of east-central Alabama, only minimal soil 

development is present in Holocene age alluvium that 

undergoes periodic flooding and sediment attrition. 

Some of the characteristic properties of these soils are 

(1) the dominance of Bw horizons rather than argillic 

horizons, (2) the irregular decrease in organic carbon 

and relatively high values (>0.2 percent) of organic 

carbon to depths of 150 cm or more, (3) the nonsystematic decrease of SiO2 relative to zirconium, and 

(4) the constancy of the Fe2O3 values with depth in 

each pedon.

4. Field and laboratory data indicate that all four sites 

should be classified as Fluventic Dystrochrepts. This 

determination was not arrived at by applying the key 

to soil orders as now used in Soil Taxonomy (Soil 

Survey Staff, 1975) but through field observations of 

the soils and the parent material at each site and as a 

result of laboratory analyses. The dilemma posed in 

classifying these fluvial soils needs to be addressed by 

soil taxonomists.

REFERENCES CITED

Altschuler, Z.S., Dwornik, E.J., and Kramer, H., 1963, Transformation of montmorillonite to kaolinite during weathering: 

Science, v. 141, p. 148-152.

Birkeland, P.W., 1984, Soils and geomorphology: New York, 

Oxford University Press, 372 p.

Harden, J.W., 1987, Soils developed in granitic alluvium near 

Merced, California: U.S. Geological Survey Bulletin 1590- 

A, 65 p.

Karathanasis, A.D. 1982, Characteristics of naturally acid soil 

smectites: Auburn, Ala., Auburn University, unpublished 

Ph. D thesis, 217 p.

Karathanasis A.D., and Hajek, B.F., 1983, Transformation of 

smectite to kaolinite in naturally acid soil systems: Structural 

and thermodynamic considerations: Soil Science Society of 

America Journal, v. 47, no. 1, p. 158-163.

Linsley, R.K., Jr., Kohler, M.A., and Paulhus, J.L., 1975, 

Hydrology for engineers: New York, McGraw-Hill, 482 p.

Markewich, H.W., and Christopher, R.A., 1982a, Pleistocene(?) 

and Holocene fluvial history of Uphapee Creek, Macon 

County, Alabama: U.S. Geological Survey Bulletin 1522,16 

P-

 1982b, Geologic map of the LaPlace and Tuskegee 

Quadrangles, Macon, Tallapoosa, and Elmore Counties, 

Alabama: U.S. Geological Survey Miscellaneous Investigations Map 1-1417, scale 1:48,000.

Nettleton, W.D., Flach, K.W., and Brasher, B.R., 1969, Argillic 

horizons without clay skins: Soil Science Society of America 

Journal, v. 33, no. 1, p. 121-125.

Nikiforoff, C.C., 1949, Weathering and soil evolution: Soil 

Science, v. 67, p. 219-230.

Shipp, D.L., 1985, A floristic analysis of Holocene leaf mats from 

Macon County, Alabama: Fairfax, Va., George Mason 

University, unpublished M.Sc. thesis, 138 p.

Soil Survey Staff, 1972, Soil Survey investigations report no. 1: 

Soil Survey laboratory methods and procedures for collecting 

samples: Washington, D.C., U.S. Department of Agriculture, 

Soil Conservation Service, 63 p.

 1975, Soil taxonomy: Washington, D.C., U.S. Department of Agriculture, Soil Conservation Service, Agriculture 

Handbook No. 436, 754 p.

 1981, Soil Survey manual no. 1: Washington, D.C., U.S. 

Department of Agriculture, Soil Conservation Service, 

unpublished revision of Agriculture Handbook No. 18,107 

P1986, Designations for master horizons and layers in

soils: New York, Cornell University, Department of 

Agronomy, 16 p.

Sudom, M.D., and Arnaud, R.J., 1971, Use of quartz, zirconium, 

and titanium as indices in pedological studies: Canadian 

Journal of Soil Science, v. 51, p. 385-396.

Analyses of Four Holocene Inceptisols in Alabama C13

Tables 1-7
Table 1. Analytical methods and units of expression for 

analyses conducted at the Soil Conservation Service National 

Soil Survey Laboratory, Lincoln, Nebr.

Analysis

Particle size .................

Organic carbon............

Dithionite-citrate ........

Iron.............. .................

Aluminum ...................

Manganese ...................

Bulk density .............

COLE2..... ..............

15-bar tension....... ......

WRD3 . ...........

Extractable bases... . ..

CEC4:

Sum of cations....

NH 4OAC ......

A1+ bases..............

Base saturation:

Sum of cations ..

NH4OAC .......

pH:

CaCl-, ................

H,O .......................

Method

code 1

...3A1

...6A1C

....6C2A

....6C2B

....6G7A

...6D2A

...4A1D

4Dl

. .4B2A

..4Cl

....5B5A

....5A3A

.. 5A8B

..5A3B

....5C3

... 5Cl

..8C1C

...8C1A

Unit of expression

Weight percent <2-mm material

Weight percent <2-mm material

Weight percent <2-mm material

Weight percent <2-mm material

Weight percent <2-mm material

Weight percent <2-mm material

g/cm3 <2-mm material

cm/ cm whole soil

Weight percent <2-mm material

cm/ cm whole soil

meq/ 1 00 g <2-mm material

meq/ 1 00 g <2 mm-material

meq/ 100 g <2 mm- material

meq/ 100 g <2 mm-material

Percent

Percent

Negative Iog 10

Negative log ]0

VPV staff no~n\

Coefficient of linear extensibility. 

Water-retention difference. 

Cation exchange capacity.

C16 Pedologic Studies in the Eastern United States
Table 2A. Field description of pedon S81AL- 087-001

[The Uphapee Creek A soil is developed in Holocene-age fluvial sediments and is classified as a fine loamy, mixed, thermic Fluventic 

Dystrochrept. The series is undesignated but was considered on the basis of field evidence to be closest to Riverview. Site location is in Macon 

County, Alabama, inSE/4, sec. 17, T. 17N., R. 24 E. ,Tuskegee 7.5-minute quadrangle, on the flood plain of Uphapee Creek. The altitude of the 

site is 255 ft (78 m) above sea level. A radiocarbon age of 7.500 yr B.P. (Markewich and Christopher, 1982a) was obtained from wood in a layer 

of organic detritus from near the base of the alluvial sediments about 500 ft (150 m) from the sample locality. The width of the Hood plain at this 

locality is about 0.75 to 1 mi (1-1.6 km). No entry, no data]

Depth

(cm)

0-26 .............

26-47 ......... .

47-73 ..

73-97 ...........

97-115.........

115-130.......

130-170.... .

170-200.......

Horizon

........Ap(Ap)

....... B21 (Bwl)

...... B22(Bw2)

B23t(Bw3)

B24(Bw4)

.63 (BC)

.... IIC1 (Cl)

.....1IC2(C2)

Moist 

color^

10YR4/3 

10YR5/3 

10YR4/3 3 , 10YR2/ I 3 

10YR 5/4 

7.5YR 5/43 

7.5YR4/4 

10YR5/63 , 10YR5/2 3 

10YR5/6 

10YR6/2 3 , 10YR5/8 3 

10YR5/6 

10YR6/1 3 , 10YR6/8 3 

10YR6/6 

10YR6/3 3 , 10YR6/1 3 

10YR7/2 (uncoated) 

7.5 YR 4/4 (coated)

Texture

fsl 

fsl

fsl 

cl 

vfsl 

fsl 

Ifs 

fs

Structure

Imsbk 

3mpr, Imsbk

Imsbk, 2msbk 

2msbk 

2msbk 

Imsbk 

MA 

SG

Clay 

skins Roots Boundary"

None 

None

None

None 

None 

None 

None

cw 

cw

as 

cs 

cw 

gw 

as

^ New hori/on designations, taken from Soil Conservation Service (1986), are given in parentheses. 

^Munsell notation. 

3 Mottles.

fsl. fine sandy loam; cl, clay loam; vfsl, very fine sandy loam; Ifs, loamy fine sand; fs, fine sand. 

.?!, weak; 2, moderate; 3. strong; m, medium; sbk, subangular blocky; pr, prismatic; MA, massive; SG, single grain.

cw, clear wavy; as, abrupt smooth; cs, clear smooth; gw, gradual wavy.

Table 28. Textural analysis of pedon S81AL-087-001

[Grain si/e in millimeters; all other values in weight percent. VF, very tine; F, fine; M, medium; C, coarse; VC, very coarse; 

detectable limits; TR, trace]

. analy/ed but below

Depth 

(cm)

0-26 ... ...........

26-47 .. ..........

47-73 .............

73-97 .............

97-1 15 ...........

115-130........

130-170.........

170-200.........

Horizon 1

... .....Ap(Ap)

....... B21 (Bwl)

.........B22 (Bw2)

.......B23t(Bw3)

.........B24 (Bw4)

......... B3 (BC)

.........IIC1 (Cl)

.........IIC2(C2)

Clay 

(<.002)

7.4

12.2

11.7

27.1

22.5

16.7

8.5

1.2

Total

Silt 

(.002- 

.05)

24.7

21.4

16.7

31.8

34.6

21.9

8.5

4.4

(.05- 

2)

67.9

66.4

71.6

41.1

42.9

61.4

83.0

94.4

Clay

F

(<.0002)

3 3

2.8

4.1

15 ">

11.9

8.5

6.5

Silt

F

(.002- 

.02)

7.8

6.5

4.5

12.3

11.4

5.7

.8

.4

C

(.02- 

.05)

16.9

14.9

12.2

19.5

23.2

16.3

7.7

4.0

VF 

(.05- 

.10)

49. 1

46.4

44.4

29.8

3 1. 3

33.8

42.8

1 3. 2

F 

(.10-

 25)

I6.l

17. 1

24.1

6.6

8.9

25.8

28.4

31.3

Sand

M 

(.25- 

.50)

1.7

1.9

2.0

3.1

1.4

1.6

10.5

33.4

C

(.50- 

1.0)

0.8

.9

l.O

1. 4

1. 2

.2

1. 3

14.4

VC

(1.0- 

2.0)

0.2

.1

.1

.2

.1

TR

TR

2.1

New hori/on designations, taken from Soil Conservation Service (1986), are given in parentheses.

Analyses of Four Holocene Inceptisols in Alabama C17
Table 2C. Physical and chemical analyses of pedon S81AL-087-001

[Units of measure for all values given in table I. - -, not detected; TR, trace]

Dithionite-citrate

Depth

(cm)

0-26 ................

26-47 ..............

47-73 ..............

73-97 ..............

97-H5. ...........

1 15-130... .......

130-170 .... ......

170-200.........

Depth

(cm)

0-26 ..............

26-47 .............

47-73 .............

73-97 .............

97-115 ..........

115-130.......

130-170........

170-200.........

Depth

(cm)

0-26 .............

26-47 .............

47-73 .............

73-97 .............

97-115..........

115-130.........

130-170.........

170-200 .........

Horizon

..........Ap (Ap)

..........B21 (Bwl)

..........B22 (Bw2)

..........B23t(Bw3)

..........B24 (Bw4)

........ B3 (BC)

..........IIC1 (Cl)

.........IIC2(C2)

Organic 

C

0.82 

.45 

.29 

.30 

.25 

.21 

.16 

.14

Total Extractable 

N Fe

0.065 

.034 

.023 

.034

0.3 

.4 

.3 

.8 

.6 

.4 

.2 

.1

Water content

Horizon

An 1 An\

.........B21 (Bwl)

..........B22 (Bw2)

....... ..B23t(Bw3)

...... ...B24 (Bw4)

. . ... ..B3 (BC)

... ...... IICI (Cl)

. .IIC2(C2)

Horizon 1

..........Ap (Ap)

....... ..B2l (B\vl)

..........B22 (Bw2)

.......... B23t(Bw3)

.........B24 (Bw4)

..........B3 (BC)

IICI (Cl)

..........IIC2(C2)

1/3 bar

12.2 

12.6 

11.8 

22.9 

20.6 

13.9 

10.3 

8.8

Sum of 

cations

6.3 

5.8 

5.3 

13.2 

13.2 

9.2 

4.9 

1.3

15 bar 3

4.2 

4.9 

4.5 

1 0.3 

8.9 

6. 1 

2.6 

1. 1

CEC 2

NH 4OAC

5.8 

5.4 

5.2 

12.7 

10.9 

7.6 

3.3 

1.1

WRD5

0.12 

.10 

.10 

.18 

.17 

.12 

.11 

.12

Bases + 

Al

4.3 

4.4 

4.4 

10.6 

9.3 

6.2 

2.7 

.9

 Fxtrartahle Rat.o clay

Al CEC 2 15 bar 3

O.I 0.78 0.57 

. I .44 .40 

.1 .44 .38 

.2 .47 .38 

.2 .48 .40 

.1 .46 .37 

.1 .39 .31 

TR .92 .92

NH4OAC extractable bases

Bulk density

1/3 bar

.46 

.36 

.43 

.42 

.48 

.53 

.46 

.51

Sum of 

Ca Mg Na K bases

3.3 0.5 TR 0.2 

2.4 .3 -- .1 

.5 .1 -- .2 

5 2 1

.1 .2 TR .1 

TR .2 TR .1 

.1 TR .1

TR TR TR

yyl Base saturation

saturation Sum NH 4OAC

7 63 69 

36 48 52 

82 15 15 

92 6 6 

96 3 4 

95 3 4 

93 4 6 

100 -- 2

4.0

2.8 

.8 

.8 

.4 

.3 

.2 

TR

KCI

4.3 

4.0

3.8 

3.5 

3.4 

3.4 

3.7 

3.9

Oven dry

.47 

.37 

.43 

.51 

.53 

.55 

.47 

.51

COLE4

0.002 

.002

.021 

.011 

.004 

.002

Extractable 

Acidity Al

2.3 

3.0 

4.5 

12.4 

12.8 

8.9 

4.7 

1.3

pH

CaCl 2 

(1:2)

4.6 

4.6 

4.0 

4.2 

4. 1 

4.3 

3.9 

4. 1

0.3 

1.6 

3.6 

9.8 

8.9 

5.9 

2.5 

.9

H 2O

(1:1)

5.4

5.2 

4.7 

4.5 

4.5 

4.5 

4.5 

4.7

New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses. 

Cation exchange capacity. 

Water content at 15-bar pressure. 

Coefficient of linear extensibility. 

Water-retention difference.

C18 Pedologic Studies in the Eastern United States
Table 2D. Optical mineralogy of very fine sand fraction of 

selected horizons of pedon S81AL-087-001

[Potassium feldspar is the dominant weatherable mineral in all horizons, 

tor both count and adjusted count. TR, trace]

Mineral

Count 

(percent)

Adjusted count 

(percent)

Horizon B21 (Bwl), 1 26-47 cm, very fine sand

Quartz ............... . .................. 78 78

Potassium feldspar............... 19 19

Opaques ......... ..... . .. .... ......... 1 I

Plant opal ........ ................ 1 1

Hornblende ..... ................. 1 I

Kaolinite.......... ........... . TR TR

Tourmaline .............................. TR TR

Muscovite ............. . TR TR

Epidote ............................ ... ... TR TR

1 otal resistant.............. ......... 80 80

Horizon B23I (Bw3), 1 73-97 cm, very fine sand

Quartz. .. ........................ . 77 77

Potassium feldspar............... .. 19 19

Muscovite .... ................ ......... . 2 TR

Opaques ... ................ ...... .......... ..2 2

Tourmaline ................................ TR TR

Zircon ...................................... TR TR

Hornblende................................. TR TR

Kaolinite.................................... TR TR

Total resistant............................. 79 81

Horizon 2C2 (C2), 1 170-200 cm, very fine sand

Quart/.. .................._............ 82 83

Potassium feldspar................ 14 14

Opaques . ...................... ......... . 1 1

Muscovite ................................. 1 TR

Rutile .. ...................................... TR TR

Zircon .... .................................. TR TR

Tourmaline ...... ...................... . TR TR

Epidote ....................... TR TR

Biotite . .................................. TR TR

T otal resistant............................. 83 84

New horizon designations, taken from Soil Conservation Service 

; 1986). are in parentheses.

Table 2f. Bulk chemistry of pedon S81AL-087-001

[All values in weight percent except for Fe->() ,/ Al-,0-,, which is a ratio. New horizon designations, taken from Soil Conservation Service (I986), are in 

parentheses]

Major oxide

Horizon

AP(Ap) B21(Bw1) B22 (Bw2) B23t (Bw3) B24 (Bw4) B3 (BC) 2C1 (C1) 2C2 (C2)

SiO2 .... 

A 1 2 03 . 

Fe 2 03 

CaO ... 

K0 ....

MnO .................

Fe 2O 3 /Al 2O 3 .

86.9 

6.4

1.1

2

1.9

.7

.04

.17

36.7 

6.7 

1.2

.2 

1.8

.7

.04

.18

87.9 

6.4 

1.2 

.2 

1.6 

.7 

.05 

.19

77.7 

11.0 

2.6 

.2 

1.8 

.8 

.05 

.24

80.0 

10.0 

2.2 

.1 

1.9 

.8 

.12 

.22

85.2 

7.2

1.6 

.1

1.7 

.7 

.02 

.22

82.1 

9.5 

2.2 

.3 

2.4 

1.6 

.08 

.23

83.1 

8.7

2.4 

.3

2.5

1.7

.1

Analyses of Four Holocene Inceptisols in Alabama C19
Table 3/\. Field description of pedon S81AL-087-002

[The Uphapee Creek B soil is developed in Holocene-age fluvial sediments and was classified on the basis of field evidence as a clayey mixed, 

thermic Aquic Paleudult (data support clayey, mixed, thermic Hapludult or Ochraquult). The series is undesignated. Site 2 is located at the 

section corner of sees. 1,2, I l.and 12. Forthis report, it is located atanaltitude of 242 ft (74m) above sea level, Tuskegee 7.5-minute quadrangle, 

20+ ft (7 m) north of Uphapee Creek, sec. 1, T. 17 N., R. 23 E., Macon County, Alabama. Wood from organic debris exposed in the bank of 

Uphapee Creek at the base of the alluvium terrace level has been dated at 6.500 years (Markewich and Christopher, 1982a). This pit was pumped 

to describe the profile and repumped to sample. No entry, no data]

Depth 

(cm)

0-20 .............

20-36 ...........

36-58 ...........

58-78 ...........

78-H2.........

1 12-146 ......

1 46- 1 76 ......

206-230 ......

Moist 

Horizon^ colon

.......Al (A) 10YR3/2

.......A2(E) 10YR5/3

.......B2l (Bw) SYR 4/4

lOYR 6/24 

.......B22tb (Bwgl) 10YR6/2

SYR 5/64 

.......B23tg2 (Bwg2)IOYR6 I

5YR5/64, 7.5YR5 8 4 

........ B23tg2 (Btg I) IOYR6/1

SYR 5,64, 7.5YR 5 8 4 

....... B24t(Btg2) 10YR6/I

7.5YR5 84 

....... 11C (Cl)

Texture

fsl

fsl

cl

c

c

c

sc

g

Clay 

Structure" skins

Imgr

Imgr

Imsbk

2mabk

3cpr

3mabk 

3cpr

3mabk 

2msbk

SG

Roots Boundary7

cs

cw

cw

pc

ci

aw

'New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses. 

2 Horizon split for sampling.

Munsell notation. 

4 Mottles.

fsl, fine sandy loam; cl, clay loam; c, clay; sc, sandy clay; g, gravel.

"1, weak; 2, moderate; 3, strong; m, medium; c, coarse; gr, granular; sbk, subangular blocky; abk, angular blocky; pr, prismatic; SG, 

single grain.

cs, clear smooth; cw, clear wavy; gs, gradual smooth; ci, clear irregular; aw. abrupt wavy.

Table 3B. Textural analysis of pedon S81AL-087-002

[Grain size in millimeters; all other values in weight percent. VF, very fine; F, line; M, medium; C, coarse; VC, very coarse]

Total Silt Sand

Depth

(cm)

0-20 ...............

20-36 .............

36-58 .............

58-78 .............

78-1 12.... .......

112-146.........

146-176.........

Horizon 1

.........Al (A)

.........A2(E)

.........B2lt(Bw)

......... B22tg(Bwg I)

.........B23tg(Bwg2)

.........B23tg(Btgl)

......... B24tg(Btg2)

Clay 

(<.002)

7.8

7.3

36. 1

50. 1

'40.8

40. 1

26.6

Silt

(.002- 

.05)

26.7

26.6

24.0

20.2

20.2

16.8

I5.8

(.05-

2)

65.5

66. 1

39.9

29.7

39.0

43. 1

57.6

F 

(<.0002)

1. 7

2.4

16.8

26.5

21.4

16.5

1 4. 3

F

(.002- 

.02)

1 3.6

I5.0

1 3.6

1 3. 3

1 2.4

II. 2

I0.2

C

(.02- 

.05)

1 3. 1

1 1. 6

I0.4

6\9

7.8

5.6

5.6

VF

(.05- 

.10)

26.7

29.5

1 8.3

10.5

14.2

1 4.3

18.4

F

(.10-

.25)

19.2

19.7

11.3

8.4

11.4

13.3

17.3

M

(.25- 

.50)

7.8

7.8

5.5

6.1

7.4

10.4

13.1

C

(.50- 

1.0)

8. 1

6. 1

3.6

3.6

4.4

4.4

6.6

VC

(1.0- 

2.0)

3.7

3.0

1. 2

l.l

1. 6

.7

2.2

New horizon designations, taken from Soil Conservation Service (1986). are given in parentheses.

C20 Pedologic Studies in the Eastern United States
Table 3C. Physical and chemical analyses of pedon S81AL-087-002

[Units of measure for all values given in table I. --, not detected; no entry, not analy/ed; TR, trace]

Dithionite-citrate

Depth 

(cm)

0-20 ...... .........

20-36 ..............

36-58 ..............

58-78 ..............

8-M2 ..............

1 12-146... ......

1 46- 1 76 ......

Depth 

(cm)

0-20 ................

20-36 .... .........

36-58 ..............

58-78 ..............

78-1 12.. ..........

112-146 ..........

146-176..........

Depth 

(cm)

0-20 ................

20-36 ..............

36-58 .......... ...

58-78 ..............

78-112...........

112-146... ....

146-176.. .......

Horizon 1

.........Al (A)

..........A2(E)

.... .82 It (Bw)

......... B22tg(Bwgl)

..........B23tg(Bwg2)

.......... B23tg(Btgl)

.......... .B24t(Btg2)

Organic 

C

1. 48 

.56 

.41 

.31 

.26 

.26 

.24

Total

N

0.064 

.024 

.028 

.027

Extractabh 

Fe

0.2

.2 

.8 

1.1 

.7 

.7 

.6

W'ater content

Horizon 1

..........Al (A)

..........A2(E)

.......... B2lt(Bw)

........B22tg(Bwgl)

.......... B23tg(Bwg2)

.... ......B23tg(Btgl)

..........B24t(Btg2)

Horizon

..........Al (A)

..........A2(E)

........ B2lt (Bw)

..........B22tg(Bwgl)

......... B23tg(Bwg2)

.......... B23tg(Btg I)

... .....B24t(Btg2)

1/3 bar

I6.8 

1 3. 1 

2I.O

27.3 

23.3

21. 1

Sum of 

cations

7.6 

3.6 

13.9 

20.9 

17.0 

17.9 

13.5

15 bar3

3.4 

2.6 

1 2.9 

1 7.0 

1 3. 7 

1 3. 7 

IO.I

CEC 2

NH4OAC

6.3 

3.2 

I2.I 

18.6 

15. 1 

16.2 

12.2

WRD5

0.19 

.17 

.12 

.15 

.15

.17

Bases +

Al

2.3 

1.6 

9.3 

14.4 

11.9 

12.7 

9.6

e

Evtramblp Katl ° clay

Al CEC 2 15 bar3

O.I 0.8 1 0.44 

TR .44 .36 

.2 .34 .36

.2 .37 .34 

.2 .37 .34 

.2 .40 .34 

.1 .40 .38

NH 4OAC extractable bases

Bulk density

1/3 bar Oven dry

1. 44 

1. 63 

l.5l 

1. 47 

1. 53 

1. 50 

l.6l

Sum of 

Ca Mg Na K bases

0.4 0.3 0.1 0 

.3 .2 .1 

1.3 1.2 TR .2 2 

.9 1.7 TR .2 2. 

.1 1.0 .1 .2 1 

TR 1.0 TR .2 1 

TR .5 .1 .1

A l Base saturation

saturation Sum NH4OAC

65 11 13 

63 17 19 

71 19 22 

81 13 15 

88 8 9 

91 7 7 

93 5 6

.8 

.6

.7 

.8 

.4 

2

.7

KCI

3.8 

3.9 

3.4 

3.3 

3.3 

3.2 

3. 1

1. 46 

1. 64 

1. 67 

1. 75 

1. 69

1. 76

COLE4

0.005 

.002 

.034 

.059 

.033

.030

Extractable 

Acidity Al

6.8 

3.0 

M.O 

I8.I 

15.6 

16.7 

1 2.8

P H

CaCI 2

(1:2)

4.5 

4.7 

4.4 

4. 1 

4.0 

4.0 

3.7

1. 5 

I.O 

6.6 

1 1. 6 

10.5 

II. 5 

8.9

H 2O

(1:1)

4.7 

5.0 

4.7 

4.5 

4.5 

4.3 

4.3

New hori/on designations, taken from Soil Conservation Service (I986), are given in parentheses. 

"Cation exchange capacity.

 Water content at 15-bar pressure. 

Coefficient of linear extensibility.

 Water-retention difference.

Analyses of Four Holocene Inceptisols in Alabama C21
Table 3D. Optical mineralogy of very fine sand fraction of 

selected horizons of pedon S81AL-087-002

[Potassium feldspar is the dominant weatherable mineral in all hori/ons, 

for both count and adjusted count. TR, trace]

Mineral

Count

(percent)

Adjusted count 

(percent)

Horizon B21t (Bw), 1 22-47 cm, very fine sand

Quartz........................................... 80 81

Potassium feldspar.................... 16 17

Muscovite ................................. 2 TR

Opaques.......................................... 1 1

Epidote............................................ 1 1

Zircon........................................... TR TR

Kaolinite......................................... TR TR

Rutile............................................. TR TR

Plant opal .................................... TR TR

Total resistant................................ 81 82

Horizon B23tg (Bwg2), 1 78-112 cm, very fine sand

Quartz............................................ 80 82

Potassium feldspar...................... 15 15

Muscovite ...................................... 3 TR

Zircon.............................................. 1 1

Opaques.......................................... 1 1

Tourmaline.................................... TR TR

Epidote............................................ TR TR

Plant opal ...................................... TR TR

Total resistant................................ 82 84

New horizon designations, taken from Soil Conservation Service 

(1986), are in parentheses.

Table 3f. Bulk chemistry of pedon S81AL-087-002

[All values in weight percent except for Fe 2O^/Al 2O V which is a ratio. New hori/on designations, taken from Soil Conservation Service (1986), are

in parentheses]

Horizon

Major oxide A1 (A) A2(E) B21t (Bw) B22tg (Bwgl) B23tg (Bwg2) B23tg (Btgl) B24t (Btg2) 2C

SiO2 ....

A1 203

Fe 203

CaO....

K 2O....

TiO2 ...

MnO

83.9 

9.4 

1.3 

.3 

2.7 

1.6

Fe2O3 / A1 2O3 ............................. .14

84.3

9.3

1.3 

.3

2.7

1.7 

.06 

.14

70.5 

19.2 

4.1 

.3 

2.1 

1.3 

.03 

.21

64.4

23.7 

5.4 

.3 

1.7 

1.2 

.02 

.23

67.4 

21.9 

4.2 

.2 

1.9 

1.3 

.03 

.19

67.2 

21.4 

4.9 

.2 

1.9 

1.2 

.03 

.23

68.8 

20.3 

4.5 

.2 

2.0 

1.2 

.03 

.22

75.4

16.0

2.5

.25

2.2

1.4

.04

.16

C22 Pedologic Studies in the Eastern United States
Table 4A Field description of pedon S81AL-101-001

[The Tallapoosa River A soil is developed in Holocene-age fluvial sediments and was classified in the field as a fine silty siliceous, thermic Typic 

Hapludult. The stud\ site is located at an altitude of 170 ft (52 m) above sea level in NW'4, sec. 3, T. 16 N., R. 20 E.. Montgomery County, 

Alabama, Mount Meigs 15-minute quadrangle. A radiocarbon date from this locality is 6,520 yr B.P. on disseminated carbon exposed at the 

base of the alluvium along the Tallapoosa River, approximately 100 yd (91 m) from the study site (Markewich and Christopher, I982a). No 

entr\. no data]

Depth 

(cm)

0-22 ......... .

22-47 .. ...

47-66 ..........

66-89 ...........

89- 1 23 .........

1 23-16 1 .......

161-190.....

190-215.....

Horizon

.......Ap(Ap)

.......B2lt 2 (Bw)

.......B21t 2 (BtI)

........ B22(Bt2)

........ B23t 2 (Bt3)

........ B23t 2 (Bt3)

......B3(BC)

. ...IIC(C)

New horizon designations. 

Horizon split for sampling.

Moist 

color-'

IOYR4.3 

7.5YR4/4 

7.5YR4 4 

IOYR 5/6 

10YR6/34, IOYR 2/ I 4 

IOYR 5/8 

10YR6/34, IOYR 2/ 1 4 

IOYR 5/8 

10YR6/34, IOYR 2/ 1 4 

7.5YR4/4 

Brown and white

Texture

sil 

sic 

sic 

sic

sicl 

sicl

1

s

taken from Soil Conservation Service (1986),

Clay 

Structure" skins

Imfgr 

2msbk 

2msbk 

2msbk

2msbk 

2msbk

Icsbk 

SG

are given in parentheses.

*J

Roots Boundary'

cw

gw 

cw

cw 

as

Munsell notation. 

4 Mottles. 

^sil, silty loam; sic, silty clay; sicl, silty clay loam; 1, loam; s, sand.

1, weak; 2, moderate; f, fine; m, medium; c, coarse;,<gr, granular; sbk, subangular blocky; SG, single grain. 

'cw, clear wavy; gw, gradual wavy; as, abrupt smooth.

Table 4B. Textural analysis of pedon S81AL-101-001

[Grain size in millimeters; all other values in weight percent. VF, very fine; F, fine; M, medium; C, coarse; VC, very coarse;

detectable limits; TR, trace]

, analyzed but below

Depth 

(cm)

0-22 ..............

22-47 ...... .......

47-66 ..............

66-89 ..............

89-123 ............

123-161 ..........

161-190..........

190-215..........

Horizon 1

..........Ap(Ap)

.......... B21t(Bw)

.......... B21t(BtJ)

.......... B22t (Bt2)

...... ...B23t(Bt3)

.......... B23t(Bt3)

....... ...B3 (BC)

.......... IIC (C)

Clay 

(<.002)

14.8

46.6

43.1

40.2

25.3

26.4

12.9

3.2

Total

Silt

(.002- 

.05)

44.8

48.1

50.5

52.1

50.1

44.4

13.8

4.8

Sand

(.05-

2)

40.4

5.3

6.4

7.7

24.6

29.2

73.6

92.0

Clay

F 

(<.0002)

8.6

23.1

16.8

16.8

8.2

9.4

8.1

.8

Silt

F

(.002- 

.02)

22.6

33.0

34.1

36.1

24.5

25.2

7.7

2.4

C

(.02- 

.05)

22.2

15.1

16.4

16.0

25.6

19.2

6.1

2.4

VF

(.05- 

.10)

18.6

3.2

5.8

7.0

22.9

20.2

18. 9

1.1

F

(.10-

.25)

1 8. 3

1. 7

.4

.6

1. 5

8.6

50.3

5.6

Sand

M

(.25- 

.50)

2.8

.3

.1

.1

.1

.2

3.7

26.9

C

(.50- 

1.0)

0.4

.1

.1

TR

.1

.1

.4

38.5

VC

(1.0- 

2.0)

0.3

TR

TR

19.9

New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses.

Analyses of Four Holocene Inceptisols in Alabama C23
Table 4C. Physical and chemical analyses of pedon S81AL-101-001

[Units of measure for all values given in table I. , not detected; TR, trace]

Dithionite-citrate

Depth 

(cm)

0-22 ................

22-47 . ............

47-66 ...... .... .

66-89 ..............

89- 1 23 ............

123-161 ..........

I6I-190 ..........

190-215.. .......

Horizon 1

..........Ap(Ap)

.......... B21t(Bw)

.......... B21t(Btl)

...... ...B22t(Bt2)

.......... B23t(Bt3)

........... B23t(Bt3)

..........B3(BC)

.......... 11C (C)

Organic 

C

1.13 

A\ 

.34

.35 

.25 

.23 

.20 

.22

Total Extractable 

N Fe

0.081 

.045 

.033 

.046

0.9 

2.2 

2.5 

2.4 

1.9 

1.9 

1.0 

.3

Fvtrartable Ratio clay

Al CEC 2 15 bar 3

O.I 0.50 0.45 

.2 .37 .38 

.3 .38 .39 

.3 .36 .40 

.2 .36 .45 

.2 .39 .43 

.1 .36 .41 

TR .44 .56

Bulk density

1/3 bar

1. 43 

1. 45 

1. 50 

1. 56 

1. 60 

1. 56 

1. 60 

1. 60

Oven dry

1. 45 

1. 60

1. 65 

l.6l

COLE4

0.005 

.033

.019 

.011

NH4OAC extractable bases

Depth 

(cm)

0-22 ................

22-47 .............

47-66 .............

66-89 ..............

89- 1 23 ...........

123-16I ..........

I62-190... .. ..

1 90-21 5.. .......

Depth 

(cm)

0-22 ...............

22-47 ..............

47-66 ..............

66-89 .............

89-123...........

123-161 ..........

161-190.........

190-215..........

Water content

Horizon

.......... Ap(Ap)

.......B21t (Bw)

.... ... B2lt(Btl)

..........B22t(Bt2)

.......... B23t(Bt3)

...........B23t(Bt3)

.... ...B3(BC)

........ 11C (C)

Horizon 1

...........Ap(Ap)

..........B21t (Bw)

.......... B21t(Btl)

........... B22t(Bt2)

........ ..B27(Bt3)

....... ...B23t(Bt3)

........... B3(BC)

......... 11C (C)

1/3 bar

21.6 

26.3

25.5 

24.1

Sum of 

cations

10.6 

18.1 

16.4 

14.7 

10.9 

11.5 

6.1 

1.9

15 bar 3

6.6 

17.6 

16.9 

1 6.0 

II. 5 

1 1. 3 

5.3 

1. 8

CEC 2

NH4OAC

7.4 

1 7.4 

16.2 

14.5 

9.2 

10.3 

4.7 

1.4

WRD5

0.21 

.13

.15 

.20

Bases + 

Al

3.7 

8.8 

7.6 

6.7 

5.2 

5.4 

3.0 

.7

Sum of 

Ca Mg Na K bases

2.6 0.8 TR 0.1 

4.1 2.4 0.1 .1 

1.8 1.8 .1 .1 

1.1 1.6 .1 .1 

.8 1.3 .1 .1 

.7 1.3 .1 .1 

.4 .7 .1 .1 

.3 .2 TR

Al Base saturation

saturation Sum NH4OAC

5 33 47 

24 37 39 

50 23 23 

57 20 20 

56 21 25 

59 19 21 

57 21 28 

29 26 36

3.5 

6.7 

3.8 

2.9 

2.3 

2.2 

1. 3 

.5

KCI

4.3 

3.5 

3.3 

3.3 

3.4 

3.3 

3.5 

4.0

Extractable 

Acidity Al

7. 1 

1 1. 4 

12.6 

ll.8 

8.6 

9.3 

4.8 

1. 4

pH

CaCI 2 

(1:2)

5.3 

4.8 

4.7 

4.7 

4.7 

4.6 

4.4 

4.5

0.2 

2.1

3.8 

3.8 

2.9 

3.2 

1.7 

_2

H 2O

(1:1)

5.5 

5.2 

5.1 

5.1 

5.1 

5.0 

5.0 

5.1

'New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses.

Cation exchange capacity.

Water content at 15-bar pressure.

Coefficient of linear extensibility. 

^Water-retention difference.

C24 Pedologic Studies in the Eastern United States
Table 4D. Optical mineralogy of very fine sand fraction of 

selected horizons of pedon S81AL-101-001 

[Muscovite is the dominant weatherable mineral in all horizons for 

count; potassium feldspar is dominant for adjusted count. TR, trace]

Mineral

Count 

(percent)

Adjusted count 

(percent)

Horizon B21t (Bw),1 22-47 cm, very fine sand

Quartz........_.................................... 65 75

Muscovite ..................................... 16 3

Potassium feldspar ................. ..10 11

Kaolinite.........---............................ 5 6

Opaques......................................... 3 3

Plant opal ...................................... 1 1

Zircon ....................... TR TR

Biotite.............................................. TR TR

Epidote......................................... TR TR

Total resistant............................. 74 85

Horizon B23t (Bt3), 1 123-161 cm, very fine sand

Quartz............................................. 62 78

Muscovite ...................................... 21 1

Potassium feldspar..................... 8 10

Biotite........................................ 4 1

Opaques.......................................... 2 3

Epidote...................................... 1 2

Kaolinite.... ..... ............. ... 1 1

Zircon.............................................. TR TR

Rutile................................................ TR TR

Plant opal ...................................... TR TR

Hornblende ..................... TR TR

Total resistant ........................... 65 82

New horizon designations, taken from Soil Conservation Service 

(1986), are in parentheses.

Table 4£. Bulk chemistry of pedon S81AL-101-001

[All values in weight percent except for Fe 2O 3/ A1 2O V which is a ratio. New horizon designations, taken from Soil Conservation Service (1986), are

in parentheses]

Horizon

Major oxide AP(Ap) B21t(Bw) B21t(Bt1) B22t (Bt2) B23t (Bt3) B23t (Bt3) B3 (BC) 2C (C)

SiO2 ..... 

A 1 203 

Fe 203 . 

CaO .... 

KO ....

MnO .................

Fe 203 /Al 203 .

78.2

12.5

3.8

0.6

2.1

1.6

0.4

.30

65.0

21.9

6.6

.4

2.4

1.3

.1

.30

64.8

22.81

7.3

.4

2.5

1.3

.08

.32

62.0

22.9

6.8

.4

2.4

1.3

.1

.30

68.7

19.1

6.4

.5

2.2

1.6

.1

.34

66.1

20.6

6.9

.4

2.4

1.5

.1

.34

65.2

20.0

7.4

.6

2.2

1.7

.2 

.37

70.3

17.9

6.0

.5

2.3

1.6

.2

.34

Analyses of Four Holocene Inceptisols in Alabama C25
Table 5A Field description of pedon S81AL-101-002

[The Tallapoosa River B soil is developed in Holocene-age alluvium dated at 5,500 yr B.P. (Markewich and Christopher, I982a). The series is 

not designated; the soil was tentatively classified on the basis of field evidence as a fine silty, mixed thermic Typic Dystrochrept. The study site is 

located in SW/4, sec. 26, T. 17 N.. R. 19 E., Montgomery County, Alabama, at an altitude of 155 ft (47 m) above sea level. Mount Meigs 

15-minute quadrangle. No entry, no data]

Depth 

(cm)

0-8..............

8-30 .. .......

30-54 .. .....

54-94 ........

94-130 ......

130-164... 

16.4-190....

Horizon 1

..........Al (A)

.........Bl (Bwl)

.......... B2l(B\v2)

.......... B22(Bw3)

.......... B23(B\v4)

.........B3(BC) 

....... C (C)

New horizon designations, 

Munsell notation.

Moist 

color^ Texture"*

10YR3 3 sil 

IOYR 5 4\ 7. SYR 5, 63 

7.5YR 5 6 sicl 

IOYR 2, I 3 

7. SYR 5, 6 sicl 

IOYR 2, I 3 

IOYR 5 6 sicl 

IOYR 2 l-\ 10YR6/43 

7. SYR 5 6 sicl 

IOYR 5 6 3, IOYR6/23 

7. SYR 5, 6 sil 

IOYR 5/6 3 , 10YR6/ I 3 

IOYR 6/3-\ IOYR 2 I 3 

IOYR 6, I 3 , IOYR 5,63 I 

7.5YR5,6-\lOYR3/3 3

taken from Soil Conservation Service (1 986),

, Clay 

Structure 5 skins Roots Boundary0

ImsbkImgr 

2csbk

2msbk

2mabk2msbk 

2mabk2msbk 

Icsbk

m

are given in parentheses.

cs 

cw 

gs 

gs 

cw 

gw

Mottles.

sil. silt loam; sicl, silty clay loam; 1, loam.

1, weak; 2, moderate; m, medium; c, coarse; sbk, subangular blocky; gr, granular; abk, angular blocky. 

"cs, clear smooth; cw, clear wavy; gs, gradual smooth; gw, gradual wavy.

Table SB. Textural analysis of pedon S81AL-101-002

[Grain size in millimeters; all other values in weight percent. VF. very fine; F, fine; M, medium; C, coarse; VC, very coarse; TR, trace]

Depth 

(cm)

0-8...................

8-30 ...............

30-54 ............

54-94 .............

94-130 ........

130-164.........

164-190.........

Horizon 1

...........A1(A)

...........Bl(Bwl)

........... B21(Bw2)

........... B22(Bw3)

........... B23(Bw4)

...........B3 (BC)

...........C (C)

Clay 

(<.002)

20.7

38.1

37.1

33.8

30.4

22.4

18.3

Total

Silt

(.002- 

.05)

41.4

50.4

48.7

54.8

39.7

31.3

38.9

(.05- 

2)

37.9

11.5

14.2

11.4

29.9

46.3

42.8

Clay

F

(<.0002)

8.4

17.0

16.9

13 2

12.7

8.6

10.6

Silt

F

(.002- 

.02)

26.4

33.1

30.9

33.8

29.6

18.7

17.5

C

(.02- 

.05)

15.0

17.3

17.8

21.0

10.1

12.6

21.4

VF

(.05- 

.10)

22. 1

8.2

10.7

9.6

17.7

34.6

26.4

F

(.10- 

.25)

13.5

2.9

3.2

1.6

7.2

11.1

15.4

Sand

M C

(.25- (.50- 

.50) 1.0)

1. 3 0.5

.3 .1

.2 .1

.2 TR

3.6 .8

.4 .1

.9 .1

VC

(1.0- 

2.0)

0.1

TR

TR

TR

.6

.1

TR

l New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses.

C26 Pedologic Studies in the Eastern United States
Table 5C. Physical and chemical analyses of pedon S81AL-101-002 

[Units of measure for all values given in table I. --, not detected; TR, trace]

Dithionite-citrate

Depth

(cm)

0-8....................

8-30 ...............

30-54 .............

54-94 .............

94-130...........

130-164.........

164-190.........

Depth 

(cm)

0-8...................

8-30 ................

30-54 ..............

54-94 ..............

94-130............

130-164..........

164-190..........

Depth 

(cm)

0-8....................

8-30 ................

30-54 ..............

54-94 ..............

94-130 ....... .....

130-164..........

164-190..........

Horizon 1

...........Al (A)

.........Bl (Bwl)

..........B2l (Bw2)

........... B22(Bw3)

........... B23(Bw4)

....... .63 (BC)

C (O

Organic 

C

3.77 

.61 

.34 

.32 

.28 

.22 

.22

Total

N

0.208 

.055 

.029 

.039

Extractabk 

Fe

1.3 

2.1 

2.1 

2.1 

2.0 

1.5 

1.4

Water content

Horizon 1

A I ( \\

..........Bl (Bwl)

...........B2l(Bw2)

...........B22(Bw3)

..........B23(Bw4)

..........B3(BC)

...........C (C)

Horizon 1

A 1 ( \\

.......... Bl (Bwl)

..........B21 (Bw2)

.......... B22(Bw 3)

..........B23(Bw4)

..........B3 (BC)

..........C (C)

1/3 bar

27. 1

28.3

23.2 

22. 1

Sum of 

cations

1 8. 3 

I5.2 

I3.4 

14. 1 

12.6 

8.9 

8.5

15 bar 3

1 2.5 

16.0 

15. 8 

15.5 

13.4 

9.7 

9.0

CEC 2

NH 4OAC

16.0 

13.3 

13.3 

13.6 

12.6 

8.6 

8.2

WRD5

0.17

.18

.21 

.20

Bases + 

Al

7.8 

6.9 

7.0 

6.4 

6.1 

4.8 

4.3

- Fxtrartable Ratio cla V

Al CEC 2 15 bar3

0.2 0.77 0.60 

.3 .35 .42 

.2 .36 .43 

.2 .40 .46 

.2 .41 .44 

.2 .38 .43 

.2 .45 .49

NH 4OAC extractable bases

Bulk

1/3 bar

1. 40 

l.4l 

1. 50 

1. 44 

1. 50 

1. 52 

1. 50

Sum of 

Ca Mg Na K bases

5.1 2.1 TR 0.4 7 

1.2 1.4 2 .1 2. 

.5 1.7 .1 .1 2 

.4 1.9 .1 .1 2. 

.4 1.8 .1 .1 2. 

.3 1.3 .1 .1 1 

.3 1.1 .1 TR 1

A l Base saturation

saturation Sum NH 4OAC

3 42 47 

58 19 22 

66 18 18 

61 18 18 

61 19 19 

63 20 21 

65 18 18

.6 

.9 

.4 

.5 

.4 

.8 

.5

KCI

4.3 

3.5 

3.3 

3.3 

3.2 

3.3 

3.3

density

Oven dry

1. 64 

1. 56

1. 57 

1. 54

COLE4

0.028 

.027

.Oil 

.Oil

Extractable

Acidity Al

10.7 

1 2. 3 

ll.O 

II. 6 

10.2 

7. 1 

7.0

pH

CaCI 2 

(1:2)

5.3 

4.7 

4.6 

4.7 

4.7 

4.7 

4.7

0.2 

4.0 

4.6 

3.9

3.7 

3.0 

2.8

H 2O

(1:1)

5.4 

4.8 

4.8 

4.9 

5.0 

4.9 

4.9

New horizon designations, taken from Soil Conservation Service (1986), are given in parentheses.

Cation exchange capacity. 

3Water content at 15-bar pressure. 

Coefficient of linear extensibility. 

5Water-retention difference.

Analyses of Four Holocene Inceptisols in Alabama C27
Table 5D. Optical mineralogy of very fine sand fraction of 

selected horizons of pedon S81AL-101-002 

[Muscovite is the dominant weatherable mineral in all horizons for 

count; potassium feldspar is dominant for adjusted count. TR, trace]

Count Adjusted count 

Mineral (percent) (percent)

Horizon B22 (Bw3), 1 54-94 cm, very fine sand

Quartz.............................................. 57 73

Muscovite ...................................... 25 5

Potassium feldspar...................... 8 10

Kaolinite.......................................... 5 6

Opaques.......................................... 2 3

Epidote.......................................... I 2

Plant opal ...................................... TR TR

Biotite.......................................... TR TR

Zircon.......... ............................... TR TR

Tourmaline .................................. TR TR

Hornblende................................ TR TR

Total resistant............................... 64 82

Horizon C (C), 1 164-190 cm, very fine sand

Quartz............................................. 65 77

Muscovite ...................................... 16 3

Potassium felds-par...................... 9 11

Epidote........................................... 3 3

Biotite............................................. 2 TR

Kaolinite......................................... 2 3

Opaques......................................... 2 2

Hornblende................................... 1 1

Zircon........................................... TR TR

Total resistant................................ 69 82

New horizon designations, taken from Soil Conservation Service

(1986), are in parentheses.

Table 5£. Bulk chemistry of pedon S81AL-101-002

[All values in weight percent except for Fe 2Oy A1 2O v which is a ratio. New horizon designations, taken from Soil Conservation Service

(1986), are in parentheses]

Horizon 

Major oxide A1 (A) B1(Bw1) B21 (Bw2) B22 (Bw3) B23 (Bw4) B3 (BC) C (C)

SiO2 ................................................ 71.1 64.3 65.7 65.4 70.3 69.8 72.4

A1 2O3 ............................................ 17.6 21.7 21.8 21.5 13.9 14.5 14.0

Fe 2O3 ............................................ 5.4 6.0 6.5 6.7 4.5 4.5 4.2

CaO.".............................................. .6 .4 .4 .3 .2 .4 .4

K 20............................................... 2.3 2.3 2.4 2.5 1.8 1.9 2.0

TiO.................................................. 1.6 1.3 1.4 1.4 1.0 I.I 1.1

MnO .............................................. .2 .2 .1 .1 .1 .09 .09

Fe 2O3 /A1 203 .............................. .31 .28 .30 .31, .32 .31 .30

C28 Pedologic Studies in the Eastern United States
Table 6. Intervals of maximum clay accumulation versus intervals of translocated clay

Macroscopic evidence for

clay maxima in Microscopic evidence 

Pedon fining-upward sequence for clay cutans

S81AL-087-001 ............................ Fining-upward sequence None.

between 73 and 200 cm

(see table 2B). 

S81AL-087-002 ............................ Fining-upward sequence Slight (36-58 cm).

between 58 and 176 cm Slight (78-176 cm).

(see table 3fl). 

S81AL-101-001 ............................ Fining-upward sequence Definite (47-161 cm).

between 22 and 213 cm

(see table 4B). 

S81AL-101-002 ............................ Fining-upward sequence Distinct (0-8 cm).

between 8 and 190 cm Definite (30-130 cm).

(see table 5B). Distinct (130-164 cm).

Table 7. Particle-size distribution of sand on clay-free base for 

each pedon

[VF, very fine; F. fine; M, medium; C. coarse; VC. very coarse; no entry, 

no data]

Depth

(cm) VF F

Sand

M C VC

S81 AL-087-001

0-26 ..... ...... 

26-47 ..............

47-73.............

73-97 . ... ..

97-1 15..... .......

115-130 .........

130-170.........

1 70-200.. ........

...... 53.6 17.3 

. .... 52.8 19.7

. .... 50.3 27.3

. .... 40.9 9.1

. .... 40.4 11.4

...... 40.6 31.0

...... 46.8 31.0

13.4 31.7

1.8 

2.2 

2.3 

4.2 

1.8 

1.9 

11.5 

33.8

S81AL- 087-002

0-20 .. .. .....

20-36..............

36-58 .. . .........

58-78..............

78-1 12.. ..........

1 12-146. ....... ..

146-176..........

. .... 29.0 20.8

. .... 31.8 21.3

. .... 28.6 17.7

... .. 21.0 16.8

..... 24.0 19.3

.. .. 23.9 22.2

...... 25.1 23.6

8.5 

8.4 

8.6 

12.2 

12.5 

17.4 

17.9

8.8 4.0 

6.6 3.2 

5.6 1.9 

7.2 2.2 

7.4 2.7 

7.4 1.2 

9.0 3.0

S81 AL-101-001

0-22...............

22-47...... .......

47-66...... ......

66-89.... ........

89-123.. .........

123-161 .........

161-190. ........

190-215 ..........

..... 21.8 21.5

6.0 3.2

...... 10.2 .7

...... 11.7 1.0

...... 30.7 2.0

...... 27.4 11.7

...... 21.6 57.6

1.1 5.8

3.3

4.2 

27.8 39.8 20.6

S81AL-101-002

0-8 .................

8-30...... ........

30-54 .... ... .. ..

54-94 ........ .....

94-130.. ........ 

130-164 ......... 

164-190 .........

27.9 17.0

.. .. 13.3 4.7

...... 17.0 5.1

...... 14.5 2.4

...... 25.4 10.3 

...... 44.6 14.3 

...... 32.3 18.9

5.2

-u.s OOVEWJMENT PRINTING OFFICE: 1988 - 201-933 - 226/80040 Analyses of Four Holocene Inceptisols in Alabama C29

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