Natural Radioactive Disequilibrium of the Uranium Series
GEOLOGICAL SURVEY BULLETIN 1084-A
This report concerns work done on behalf of the U. S. Atomic Energy Commission and is published with the permission of the Commission
Natural Radioactive Disequilibrium of the Uranium SeriesBy JOHN N. ROSHOLT, Jr.
CONTRIBUTIONS TO GEOCHEMISTRY
GEOLOGICAL SURVEY BULLETIN 1084-A
This report concerns work done on behalf of the U. S. Atomic Energy Commission and is published with the permission of the Commission
UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON ~. 1959
UNITED STATES DEPARTMENT OF THE INTERIOR
FRED A. SEATON, Secretary
GEOLOGICAL SURVEY
Thomas B. Nolan, Director
The Geological Survey Library has cataloged this publication as follows:
Rosholt, John Nicholas, 1923-Natural radioactive disequilibrium of the uranium series.
Washington, U. S. Govt. Print. Off., 1959.
iii, 30 p. diagrs., tables. 25 cm. (U. S. Geological Survey. Bul letin 1084-A. Contributions to geochemistry)
Bibliography: p. 29-30.
1. Radioactivity. 2. Uranium. i. Title. (Series: U. S. Geo logical Survey. Bulletin 1084-A. Series: U. S. Geological Survey. Contributions to geochemistry)
553.493
For sale by the Superintendent of Documents, U. S. Government Printing Office Washington 25, D. C. - Price 15 cents (paper cover)
CONTENTS
PageAbstract_______________________________________________________ 1Introduction._____________________________________________________ 1Acknowledgments _________________________________________________ 4Method of measurement and definition of units______________________ 4Comparisons of equivalent uranium with uranium-__-_---------_--__-- 6Classification of disequilibrium patterns._____________________________ 7Some interpretations of causes of disequilibrium.______________________ 9Summary____________________________________________ 29References..-.____________________________________________________ 29
ILLUSTKATIONS
FIGUKE 1. Classification of natural radioisotopes into groups__________ 32. Anomalies in comparison of ell to U_______________________ 53. Types of disequilibrium classified by ratios of radioisotopes__ 84. Age of uranium deposition in years as a function of the ratios
ePa23» to U, eWo to U, and eRa"8 to U.._ ~-_~ ~_ 11
TABLES
TABLE 1. Age determination based on ratio of equivalent isotope touranium__________________________________________ 12
2. Uranium-series disequilibrium analyses.____________________ 14
m
CONTRIBUTIONS TO GEOCHEMISTRY
NATURAL RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES
By JOHN N. ROSHOLT, JR.
ABSTRACT
Many radioactive samples show radioactive disequilibrium because of the numerous geochemical processes affecting ore deposits. As it is difficult to interpret disequilibria by simply comparing radiometric and chemical assay values of uranium, analyses should be made of the abundance of Pa231, Th230, Ra228, Rn222, and Pb«°.
Uranium-series disequilibria, as shown by radiochemical studies of samples representing a cross section of most of the significant present-day radioactive deposits in the United States, can be classified according to six basic types. Interpretations of the geochemical history of these types indicate that it may be possible to date uranium deposition within a theoretical range of 2,000 to 200,000 years. Ages ranging between 6,000 and 30,000 years have been calculated for several specific samples.
INTRODUCTION
In the greatly expanded search for uranium in the last 10 years, disequilibrium in radioactive ores has presented a difficult problem to geologists and prospectors. The magnitude and frequency of disequilibria have been generally underestimated, although the im portance of disequilibrium in field and laboratory counting measure ments has begun to be realized.
Very few complete studies concerning disequilibrium in radioactive deposits have been published. Variations in the protactinium: uranium ratio have been reported by Schumb, Evans, and Hastings (1939) and Wildish (1930). Ratios of Th230 to uranium in coral limestone have been reported by Barnes, Lang, and Potratz (1956). A few results of analyses of Ra226 and U in mine-dump material have been given by Phair and Levine (1953). T. W. Stern and L. R. Stieff (1959) have reported several analyses of Ra226 and U in carno- tite ores. Kuroda (1955) has provided a number of ratios of Ra223 to Ra226 in high-grade uranium minerals. Urry (1948) has reported several analyses of varved-clay samples containing radium. Other reports primarily on radium isotopes have been written by Armburst
1
2 CONTRIBUTIONS TO GEOCHEMISTRY
and Kuroda (1956), Koczy (1954), and Chlopin and Vernadsky (1932).
The purposes of this paper are to tabulate and discuss the results of a number of complete analyses of disequilibrium samples, to illus trate a proposed classification of disequilibrium patterns, to study these patterns as clues to the understanding of the geochemical history of the samples and of the deposits, and to point out some of the difficulties when simply comparing radioactivity and chemical analyses of uranium for interpreting equilibrium or disequilibrium in samples.
To make a detailed investigation of the state of radioactive equi librium in ore-grade geologic samples, several key decay products must be measured and their relative abundances evaluated. Figure 1 shows the parent isotopes and decay or daughter products of the three principal naturally occurring radioactive decay series: the U238, U235, and Th232 series. Equilibrium is attained in a radioactive series when all the daughter products decay at the same rate that they are produced from the parent isotope. Thus, at equilibrium each of these daughter products would be present in a constant proportion to its parent isotope. The loss or gain, by geologic processes, of any of certain important isotopes during the more recent part of the existence of a mineral causes disequilibrium in the proportions of the parent isotope to its daughter products. Even though a series is not in complete equilibrium, many of the immediate short-lived daughter products will be in equilibrium with their long-lived parents. Where significant disruption of equilibrium occurs the natural radioisotopes can be separated into the following major isotopes and groups of established equilibrium shown in figure 1: the uranium group, Th230 isotope, Ra226 isotope, Rn222 group, Pb210 group, and Pa231 group in the uranium series. U235 itself will remain in constant abundance with U238 (Senftle and others, 1957); thus the U235 content is determined from the uranium analyses, which includes the isotopes U238, U235, and U234 which are assumed to be present in constant abundance to each other. In addition to these, the Th232 group may be present in some rocks and ores and add to the radioactivity.
To describe adequately the long-term state of equilibrium of the uranium series, the abundances of the long-lived isotopes, U, Pa231 , Th230, and Ra226 should be known. Analysis for Rn222 and Pb210 , as well as for uranium, is desirable for investigating radioactivity anomalies, for checking the accuracy of uranium and radioactivity analyses, and for investigating emanation properties. With the exception of a few important samples, the results on ores containing significant quantities of Th232 are not included in this paper. Radiochemical assays by the author are given in table 2 at the end of the paper.
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 3
r
>xV
\.
^JF"! r
,_ -c Q oO) OtO ,_S. clD in o* to J3OJ ' .en H- o> <co orco u.co occo <tco Q.CO OQCO o.co HCO
4 CONTRIBUTIONS TO GEOCHEMISTRY
ACKNOWLEDGMENTS
Practically all the later analyses, which include the determination for Pa231 , were made by using continuously operating automatic count ing systems for parts of the alpha-activity measurements. These sys tems were designed and maintained by J. R. Dooley, without whose assistance much of this work could not have been completed at this time. This work is part of a program being conducted by the U. S. Geological Survey on behalf of the Division of Raw Materials of the U. S. Atomic Energy Commission. A preliminary summary of this paper (Rosholt, 1957a) was presented at the Second Nuclear Engineer ing and Science Conference, Philadelphia, Pa., March 11-14, 1957.
METHOD OP MEASUREMENT AND DEFINITION OP UNITS
All the daughter-product analyses were made by alpha-particle measurements after radiochemical separations of the specific elements were made with the aid of inactive carriers. The abundance of the isotopes Pa231 , Th230 , Ra226, Rn222 , and Pb210 was determined. The methods used for these analyses have been described by Rosholt (1954; 1957b).
Equivalent uranium, expressed in percent ell, is the ratio of the radioactivity of the sample to the radioactivity of a uranium-ore standard which is in equilibrium with all of its decay products. Uranium is expressed as U, in percent, and Th232 as Th232, in percent. All the decay products are expressed in percent equivalent and thus do not represent the actual amounts of these daughter products. Percent equivalent is defined as the amount, in percent, of primary parent, under the assumption of radioactive equilibrium, required to support the amount of daughter product actually present in the sample. This amount of primary parent may or may not be present in the sample. For the Th232 series, the daughter products are calculated as equivalent to Th232 and not to U.
Some graphic examples of the definition of percent equivalent are shown in figure 2. The hypothetical sample in equilibrium is one showing 1 percent uranium, 1 percent eU, and 1 percent equivalent of all of the daughter products; that is, 1 percent ePa231, 1 percent eTh230, 1 percent eRa226, and so on. Sample 143 (Texas soil) has 0.65 percent U and 0.96 percent eTh230 . This eTh230 is present in excess of the uranium content and if equilibrium were to exist between U238 and Th230, then 0.96 percent U would be required in the sample.
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES
485002 59 2
6 CONTRIBUTIONS TO GEOCHEMISTRY
Other units which could be used to express this type of result are compared below with the equivalent units. As can be seen, the use of equivalent units simplifies recording and interpreting the data.
Isotope
U238 plus U235Pa231Th230Ra22<>Rn222Pb2io
Percentequivalent
1.01.01.01.01.01.0
Percent
1. 03. 37X10-'1. 70X10-*3. 39X10-72. 15X10-124.28X10-"
10-' curiesgrams of sample
3.55. 16
3.393.393.393.39
The use of percent equivalent has other advantages besides that of illustrating or permitting direct comparison of uranium and daughter- product abundances in the sample. It also demonstrates that an overall material balance of parent isotopes and daughter products must exist in theoretical equilibrium concentrations, although not necessarily in the concentrations of parent and daughter products found in the samples selected for examination. Stated again, percent equivalent is defined as the amount, in percent, of primary parent, under the assumption of radioactive equilibrium, required to support the amount of daughter product actually present in the sample. This amount of parent does not necessarily have to be present in the disequilibrium sample; actually more or less than that amount of uranium may be present. Thus the deficient amount of uranium or the deficient amount of daughter product, in relation to its immediate parent, must exist elsewhere than in the sample analyzed. To illustrate this principle with sample 143 (fig. 2), 0.96 percent eTh230 shows that there is a deficiency of 0.96 0.65 or 0.31 percent uranium which must exist somewhere else unaccompanied by Th230 ; also, the sample is deficient of 0.76 0.24 or 0.52 percent eRn222 and 0.76 0.25 or 0.51 percent ePb210 which must exist elsewhere, unaccompanied by Ha226.
If a large enough sample is represented, the parent and all the daughter products will be present in equilibrium. However, this sample may have to be so large that it could not be collected. It also follows that the smaller the sample collected, the greater the proba bility of increasing the amount of disequilibrium found in the sample. This seldom considered assumption may be important in collecting samples.
COMPARISONS OF EQUIVALENT URANIUM WITHURANIUM
Although it is common practice to compare a sample's actual uranium content determined chemically with its equivalent uranium
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 7
(eU), misinterpretations can be made in comparing these two values alone. Radon loss is the most common anomaly and may present some misleading conclusions. Figure 2 shows some examples. Two Colorado Plateau samples (Nos. 68 and 69) in relatively good equi librium with the exception of some radon loss show eU:U ratios very similar to two other plateau samples (Nos. 22 and 24) which have a deficiency of Th230 and Ra226 together with a lesser radon loss. Thus the comparison of eU and U will not always indicate whether the sample is deficient in radon products alone or deficient in long-lived daughter products also. Some samples may even be deficient in uranium and still show a low eU:U ratio. Sample 143, of soil from Karnes County, Tex., illustrates this extreme case. The extremely high radon loss completely masks the presence of the long-lived daughters that are actually in amounts in excess of the uranium. The eU:U ratio would indicate major disequilibrium with deficient amounts of daughter products, whereas actually it is the amount of uranium that is deficient.
A routine eU analysis will not indicate the presence of low-energy alpha emitters when beta-emitting daughter products are not present in the sample. Sample 122, a marl from the Nebraska-South Dakota border, illustrates this phenomenon. The large excess of Th230 and Pa231 is not indicated at all by the eU value because of the much lower eRa226 and eRn222 content. Sample 1 (table 2) exhibits a somewhat similar isotope distribution with a large excess of Th230, but a lower excessive content of Pa231 . The eU analysis will not reveal the high Pa231 content which is evident in many samples, because of the lack of sufficient intensity of beta emission from this group.
In a routine eU analysis the radon loss may completely mask the additional radioactivity created by the presence of Th232 and its daughter products, as shown by two samples from Prince of Wales Island, Alaska. Only one is shown in figure 2, for they have very similar analyses; neither is listed in table 2 because they are primarily thorium ores, and complete disequilibrium analyses were not made on them. The eU:U ratio seems to indicate good uranium-series equilibrium, but actually the amount of Th232 and the percent equiva lent of its daughter products are greater than those in uranium. Equivalent Ra226 is also in excess of the uranium content.
CLASSIFICATION OF DISEQUILIBRIUM PATTERNS
Study of the isotope-abundance ratios of samples exhibiting signifi cant uranium-series disequilibrium shows that the various types seem to represent certain patterns. With the use of the analyses of the key isotopes U^+IJ235 , Pa231, Th230, and Ra226 it is proposed that practically all disequilibrium samples can be classified according to six
00
Equiv
ale
nt-
abundance
ra
tios
Da
ug
hte
r- p
roduct
d
eficie
ncy
Tim
e-r
ela
ted
daughte
r-pro
duct
defic
iency
O
O
FIG
URE
3. T
ypes
of d
iseq
uilib
rium
cla
ssifi
ed b
y ra
tios
of ra
dioi
soto
pes.
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 9
different types that can result from the most recent major process of alteration. The classification is shown in figure 3. The second column shows the number of samples that were analyzed and found to fall in each type; the equivalent-abundance ratios are the average values for the indicated number of samples. The first four rows of equivalent-abundance ratios, (types 0-3) show the comparison of equivalent daughter-product content to uranium content where the U:U ratio is automatically 1. The first row (type 0) represents the hypothetical sample of perfect equilibrium.
The first three types of disequilibrium have values of U in excess of eRa226 . Type 1, daughter-product deficiency, is represented by samples in which the generalized relationships are U^>ePa231!>eTh230!> eRa226 . Type 2, time-related daughter-product deficiency, is a very special kind of type 1 disequilibrium in which each of these daughter abundances must retain a specific relation with each other. This relation must be such that the amount of growth of each isotope from pure uranium, represented by the ratios of ePa231 to U, eTh230 to U, and eRa226 to U, would require the same interval of time. Type 3, Th230 deficiency, is represented by samples in which generally ePa231 5^U>eRa226!>eTh230, the key isotope being the anomalously low Th230 .
The last three types of disequilibrium have values of eRa226 in excess of U, and as the uranium content is so small, it and all the equivalent daughter-product abundances are compared to eRa226 instead of uranium, as in the first three categories. Type 4, daughter- product excess, is represented by a low uranium content. The remaining longer lived daughter products are often present in approx imately equilibrium amounts with one another. In some samples, however, the equivalent amounts of the daughter products vary con siderably from one to another. Type 5, Ra226 excess, as shown in dump material is a special case of type 4, daughter-product excess, where generally eRa226>ePa231>eTh230 which is much >U, the key isotope being the significantly excessive Ra226. Type 6, the occurrence of radium isotopes exclusively, is a peculiar and not too uncommon type of deposit in certain localities. Here Ra228, a daughter product of Th232, is commonly found with Ra226 . The radioactive components are radium isotopes and then- immediate decay products, and there is very little or no U, Th230, Pa231, or Th232.
SOME INTERPRETATIONS OF CAUSES OP DISEQUILIBRIUM
The study of the distribution of the radioactive decay products in the types of samples listed is still in its first stage; nevertheless it is
10 CONTRIBUTIONS TO GEOCHEMISTRY
possible to explain, or at least to postulate, some of the causes of disequilibrium.
Two primary processes can be involved in the type 1 ores. Uranium may have migrated to its present location at a time less than that required by its daughter products to reach approximate equilibrium, that is, less than 300,000 years ago. The alternative is that there has been preferentially greater leaching of daughter products than of uranium. The latter explanation is the more probable in carnotite and other types of deposits where uranium fixative agents such as vanadium or phosphate are also present. Samples of this kind (type 1) that do not follow the normal U>ePa231>eTh230>eRa226 pattern (with eRa226 nearly equal to or only slightly less than eTh230) indicate that some leaching of daughter products has taken place. This kind of deficiency in daughter-product distribution is shown by samples 21, 23, 40, 60, 62, 74, 81, 86, 87, 93, 104, 108, 112, 121, 142, and 144 (table 2). Ra226 has been found to be the most common, and, in most samples of this type, the only long-lived daughter product which can be leached. Deficiencies of Rn222 and Pb210 are not considered major causes of long-lived disequilibrium. When the isotope abundance is similar to that in type 2, considerable weight is thrown to the first explanation (recent deposition of uranium). This distribution is common in many of the pitchblende-type ores such as that at the Happy Jack mine. Samples 20, 22, 24, 35, 45, 47, 52, 57, 60, 61, 62, 73, 86, 87, 104, 107, 118, and 142 may represent this kind of alteration. Some of the samples may represent more recent uranium deposition than is indicated by the abundance of the isotopes (see fig. 4). That is, they may actually be type 2 material that was deposited where some older uranium minerals already existed, or uranium may have subsequently been leached out after the original, relatively recent, uranium deposition. Samples 60, 62, 86, 87, 104, and 142 could result from the combined effect of recent uranium deposition and leach ing of Ra236.
Type 2 ores are of special significance because the isotope abun dances are such that each isotope indicates nearly the same age for the uranium deposition. The required isotope abundances must match the time intervals when compared to figure 4. For the results of testing of these samples actually to represent the age of the ura nium mineral, three conditions must be met: (a) uranium free of all decay products must have been deposited in nearly nonradioactive host rock, (b) there must have been no significant leaching of uranium or long-lived daughter products after deposition, and (c) the rate of deposition must not have been too slow compared to the rate of growth of daughter products. Evaluation of the effect of some of these conditions has been made (Rosholt, 1958). Table 1 shows the
RADIOACTIVE DISEQUILIBRIUM OP THE URANIUM SERIES 11
12 CONTRIBUTIONS TO GEOCHEMISTRY
isotope ratios and the possible age of the uranium for all the samples represented by this category. Some anthropological evidence and carbon-14 measurements (Wendorf, Krieger, and Albritton, 1955) for the same stratigraphic location from which sample 141 was obtained support the premise that the age given in table 1 is of the correct order of magnitude. Type 2 disequilibrium is not very common, but increasing knowledge of favorable geochemical and geological en vironments is now providing a greater probability of locating ores of type 2 disequilibrium. Eadiochemical data and field evidence are now being accumulated for a paper devoted primarily to geochemical interpretations based on this kind of disequilibrium.
TABLE 1. Age determination based on ratio of equivalent isotope to uranium
Sample No. 1
13 14... _ 38. _ 39 53 64 _ .55-. - 66-.. 68 141
Isotope ratio
ePa2«U
0.24 .39 .10 .088 .27 .10 .45 .25 .37 .33
eTh^o ~U~
0.13 .26 .053 .022 .15 .045 .18 .15 .26 .18
eRa2*i» U
0.13 .27 .053 .021 .13 .034 .16 .10 .22 .10
Age (years) on the basis of
Pa23i
14,000 25,000 5,000 4,500
16,000 5,000
30,000 14,000 23,000 20,000
Thzso
16,000 35,000 6,000 2,500
18,000 5,000
23,000 19,000 35,000 23,000
Ra^»
18,000 38,000 9,000 4,500
18,000 6,000
22,000 15,000 31,000 15,000
' See table 2 for description of sample.
Type 3 disequilibrium is believed to be the result of rather recent deposition of uranium contaminated with significant amounts of daughter products other than Th230 , and with silica and salts. This type of disequilibrium is often the result of evaporation of solutions containing some of the long-lived isotopes, along with silica and vari ous salts. The low Th230 content must reflect the relative deficiency of this isotope in the solutions. Sample 67, a hyalite-opal, appears to have this mode of origin. Samples 78, 79, and 80, stratigraphically below three samples (75, 76, and 77) of other classes, are most prob ably of this mode of origin (R. G. Coleman, oral communication).
Many samples with anomalously high radioactivity are of type 4. In general, disequilibrium of this type, found in samples taken from an oxidized environment, is the result of leaching of uranium. Daugh ter products may possibly have been added to the host rock, but it is difficult to select samples definitely showing that this occurred. A few samples (4, 36, 37, 42, and 82) have an abnormally low eTh230 content, which may indicate daughter-product addition when one considers that type 3 samples also have a low eTh230 content. A few samples (1, 46, 49, 71, and 72) have a low ePa231 content which may have resulted because sufficient time was available for a greater frac-
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 13
tion of Pa231 than Th230 to decay after the uranium was leached. The fact that there is little eRa226 in many samples of this type does not appear to be too significant, for radium is easily leached in many different environments.
One very significant anomaly present in many samples of type 4, especially some of the high-grade black uranium minerals, is the high Pa231 content and near equilibrium abundances of U, Th230, and Ra226 . Samples 41, 59, 61, 65, 66, 68, 69, 89, and 144 show this anomaly. One explanation seems most plausible uranium and the other decay products are preferentially leached to a greater degree than protac tinium. This may be due to the greater ability of protactinium to become hydrolized and reprecipitated immediately from the leaching solutions (Elson, 1954). Additional possible evidence of this high Pa231 content in many uranium minerals is furnished by Kuroda (1955). The high ratios of Ra223 to Ra226 that are characteristic of many of the uranium minerals he analyzed may reflect a high Pa231 content.
Most of the samples represented by type 5 disequilibrium occur in pyritic ores or ore dumps and are the result of differential leaching of all components. Sulfates formed in these materials would retain the radium even though it might migrate somewhat, whereas the sul- furic acid formed would leach and remove uranium. Further dis cussion of this type of disequilibrium is presented by Phair and Levine (1953).
The occurrences of radium isotopes exclusively (type 6 disequi librium) are commonly associated with oil- and gas-field brines. Radioactive hot-spring deposits also show this type of disequilibrium. These sometimes highly radioactive deposits are the result of copre- cipitation of radium with barium sulfate, strontium sulfate, and occasionally iron hydroxide from large volumes of water. It is also believed that the reason for the deposition of radium isotopes, essen tially free of other radioactive isotopes, is that the water contained only radium as a significant radioactive component. The radium is believed to come from the pore space of the country rock from which the water is flushed. Materials containing significant amounts of Ra228 (without Th232) must be of very recent origin, less than 30 or 35 years old. Samples 28, 127, 129, and 133-140 are of materials with recent additions of radium. Further evidence that many of these materials are of recent origin is the low Pb210 content. Sample 128 is a drill cutting from a depth of 2,530 feet and was obtained from rock below a well which was first drilled approximately 25 years ago (A. P. Pierce, oral communication). The well was deepened recently when the sample was collected. The ratio of Pb210 to Ra226 yields an age of 24 years. Further work describing many of the other aspects of oil-field radioactivity is presented by Gott and Hill (1953).
485002 59 3
TAB
LE 2
. U
rani
um-s
erie
s di
sequ
ilib
rium
ana
lyse
s ar
rang
ed b
y ge
ogra
phic
al l
ocat
ion
of t
he s
ampl
es
Sam
ple
num
ber:
Sam
ples
col
lect
ed o
r su
bmit
ted
by t
he f
ollo
win
g:
(U.
S. G
eolo
gica
l Su
rvey
unl
ess
othe
rwis
e in
dica
ted)
: E
. R
. L
andi
s, 1
; R
. U
. K
ing,
3-5
; F.
B.
Moo
re,
6-S;
B.
F.
Leo
nard
, 9,1
0; A
very
Dra
ke,
11,1
2; E
. W
. G
rutt
, Jr.
, AE
C,
13,1
4, 8
1-83
, 87
, 89
, 91
, 93
-98,
119
; C
. T
. Pi
erso
n, 1
8, 1
9; R
. A
. L
avor
ty,
AE
C,
20, 2
1, 9
9; C
. M
. T
scha
nz.
27, 2
9-32
; Hel
en C
anno
n, 2
8; R
. D
L
ynn,
Ana
cond
a C
oppe
r C
o.,
33, 3
4; S
. R
. A
usti
n, A
EC
, 35
-42;
H.
G.
Stev
ens,
43;
R.
T.
Che
w a
nd A
. F
. T
rite
s, 4
4-66
; R
. G
. L
ewis
, 67
;A
. J.
Froe
lich,
70;
W. J
. C
arr,
71,
72;
H.
E. N
elso
n, 7
3, 7
4; R
. G
. C
olem
an, 7
5-80
; J.
G. S
teve
ns,
AE
C,
84-8
6; D
. F
. D
avid
son,
88,
90;
W.
N.
Shar
p, 9
2; W
. J.
Map
el,
100;
P.
L;
Wei
s, 1
01;
J. R
. G
ill,
104,
117
, 11
8, 1
20;
D.
E.
Peac
ock,
105
, 10
6; E
. G
. E
thim
ou,
107;
G.
B.
Got
t, 10
8,11
4-11
6; E
. V
Po
st,
109;
R.
S. J
ones
, 11
0-11
3; R
. J.
Dun
ham
, 12
1-12
4,F.
W.
Stea
d, 1
25; A
. P
. Pi
erce
, 128
-130
, 13
2-13
6; J
. W
. Hill
, 13
1; R
. T
. R
usse
ll, A
EC
, 13
7,13
8; H
. J.
Hyd
en,
139;
D.
H.
Ear
gle,
141
; F.
C.
Can
ney,
142
; and
P.
F. F
ix,
143-
145.
et
T (p
erce
nt):
The
equ
ival
ent u
rani
um (
eU)
assa
ys w
ere
perf
orm
ed b
y C
. G
. A
ngel
o, S
. P
. F
urm
an,
and
D.
L.
Scha
efer
, U
. S.
Geo
logi
cal
Surv
ey.
U (
perc
ent)
: T
he u
rani
um a
naly
ses
wer
e pe
rfor
med
by
staf
f m
embe
rs o
f the
U.
S. G
eolo
gica
l Su
rvey
. P
a831
(per
cent
equ
ival
ent)
: P
a2'1
was
not
det
erm
ined
in
the
earl
y an
alys
es.
Sam
ple
No.
Lab
orat
ory
No.
Fie
ld N
o.D
escr
iptio
n an
d lo
catio
nD
is
equi
lib
ri
um
type
Per
cent
eUU
Th»
2
Per
cent
equ
ival
ent
Pa23
iT
h230
Ha
Rn22
2Pb
2">
Ha*
"
CO
LO
RA
DO
B
ent
Cou
nty
2250
91L
CR
-12
6fr
om s
ands
tone
rid
ge i
n va
lley
subj
ect
toco
nsid
erab
le w
eath
erin
g, s
ec. 3
2, T
. 27
S.,
R.
51 W
.
41.
40.
057
1.9
5.5
3.9
2.6
1.93
Las
Ani
mas
Cou
nty
223
9443
F 4
3770
ferr
ugin
ous
and
man
gano
us
subs
tanc
e;
Clif
f M
arti
n cl
aim
s ne
ar M
odel
, C
olo.
60.
620.
0002
<0.0
1<0
.002
1.84
0.87
0.72
<0.
01
Jeff
erso
n C
ount
y
3 4 K
2245
42
2186
88
RU
K-1
-55
RU
K-2
5-5
4
GA
-lb
tite
vei
n i
n b
recc
ia r
eef
at s
urfa
ce.
Fo
ot
hi
lls
Min
ing
Co.
, W
right
leas
e nea
r Id
le-
dal
e, N
EJi
, N
WM
, se
c. 3
2, T
. 4
S.,
R.
71 W
.
min
e, s
ec.
25,
T.
4 S
., R
. 71
W.
Ben
ton
fa
ult
co
nta
ct,
Tu
cker
G
ulc
h,
nort
hw
est
of G
olde
n, s
ec
21,
T.
3 S
., R
. 70
W.
4 4 4
0.06
5
.21
.082
0.00
2
.026
.019
0.13 .30
0.12 .14
.22
0.13 3f
i
.17
0.10 .33
.12
0.09
5
.29
.10
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 15
|
_< 00CO IO OJ ^J
o
S op O> 5 o
o
C i-H O i-t SO0 ...
c o o o 01o
;
i
g 8 S S fe0
rH Ih- IO to OO O O 0 *C5 ...
« « « » »
ump sample of vein material showing tel- luride and radioactive material in altered
monzonite. X-ray mine,
ample of shear-zone quartz vein, 320 ft from portal. Host rock in mine is Ter tiary monzonite. Shirley mine, NWM,
sec. 19, T. 1 S., R. 73 W. 1^-ft.
ne-ft sample of shear-zone quartz vein,
480 ft from portal. Shirley mine,
hip channel of 6-in. vein material in Gold
Hill mining area,
^lected pieces of most radioactive material,
same location as No. 9.
P oa 0 0 w
3 eq S «J
^ *H ^ ^ PRft, fr ft, K W
i-i eo t>- eo CDr-» _ i ,_| %Z ^Th Th "T^ OO OO
to b* co o» o
1_a
O
S 3o
i-l CO tO Oi
o
to Co0
CJ
0
o
CO t-« to0
*
ne-fourth-inch pitchblende veinlet in foot- wall at level 6, east, 424 ft from shaft, Old Town mine,Central City district. Mine
drains through level 22 of Argo tunnel. Abundant pyrite has produced highly
sulfate acid waters,
ne-fourth-inch sample of pitchblende veinlet which extends 4 in. along dip length between hanging wall and foot- wall branches at shaft 20 ft above level 7.
Old Town mine.
0 0
t ?£-< EH0 0
0. 00
O) O)t^ t~
,-H Ol
Gi
CO *
0 0
o
Oi toi s0
I io
S CO o
o
01 t-0 0
0
to IM
o
"O Ci« 00 -I O
o
«
edium-grained dark-green to buff sand stone with abundant limonite specks from Browns Park formation at 80- to 82- ft depth of drill hole 5470-3020, Gertrude
claims, sec. 17, T. 7 N., R. 94 W.
ssentially same type of rock as no. 13, 82-
to 84-ft depth, drill hole 5470-3020.
& W
0 S
CO CO
, 1OJ C^N N
CO "tf t-H rH
TAB
LE 2
. U
rani
um-s
erie
s di
sequ
ilib
rium
ana
lyse
s ar
rang
ed b
y ge
ogra
phic
al l
ocat
ion
of t
he s
am
ple
s C
onti
nued
Sam
ple
No.
Lab
orat
ory
No.
Fie
ld N
o.D
escr
iptio
n an
d lo
catio
nD
is
equi
lib
rium
ty
pe
Per
cent
eUU
Th-
Per
cent
equ
ival
ent
Pa23
1T
h230
Ra22
0B
n»
Pb-
Ra2
2,
CO
LO
RA
DO
Con
tinu
ed
Q
Fre
mon
t C
ount
y 8
15
16
17
2264
19
2264
21
2049
95
F-32
387
F-32
389
F-19
831
Hot
-spr
ing
sint
er;
grab
sam
ple
near
spr
ing
on A
. E
. Jam
es c
laim
alo
ng S
alt
Cre
ek.
Hot
-spr
ing
sint
er;
grab
sam
ple
near
spr
ing
on A
. E
. Ja
mes
cla
im a
long
Sal
t C
reek
. Ir
on-s
tain
ed
Dak
ota
sand
ston
e fr
om
Co-
le
xco
clai
ms,
Gar
den
Par
k di
stri
ct, n
orth
of
Can
on C
ity.
6 6 4
0.16
.15
.15
0.00
07
.003
.080
<0.
01<
0.00
5
<.0
03
.15
1.12
1.69
.16
0.07
.06
.14
0.70
.86
.13
hi<o
. 01
£j
< 01
w M
.....
* 00
Sagu
ache
Cou
nty
18
1995
756
9753
953
-P-1
6A
53-P
-99A
Pyr
itic
ore
; R
awle
y m
ine,
Bon
anza
dis
tric
t.4 4
0.75
.2
20.
59
.055
0.99
.2
91.
09
.28
Mes
a C
ount
y
20
21
2218
12
2218
13
1376
1376
A
Mill
fee
d, c
arno
tite
ore
; C
limax
Ura
nium
C
o. m
ill,
Gra
nd J
unct
ion.
..
...d
o - - -- --
-
1 1
0.33
.28
0.46
.31
0.40
.30
0.42
.28
0.29
.27
0.38
.29
Mon
tros
e C
ount
y
22
23
24
25 26
2226
36
2231
73
2231
75
1358
48
1358
51
LP
-116
8-2
LP-
1361
L
P-13
61
LP-
531-
198
LP
-530
-85
Dri
ll co
re 3
54.8
to 3
55.8
ft;
Lon
g P
ark
....
..
Dri
ll co
re 3
89.8
to
390.
4 ft;
Lon
g P
ark
....
..D
rill
core
203
.82
to 2
04.7
2 ft
; L
ong
Par
k....
Dri
ll c
ore,
car
notit
e or
e, 2
77.0
4 to
277
.35
ft;
Lon
g P
ark.
1 1 1 4 0
0.78
.0
95
.18
.007
.21
0.95
.1
8 .2
5 .0
034
.26
0.18
.2
6 .0
18
.26
0.75
.1
2 .2
0 .0
12
.26
0.74
.0
57
.20
.008
5 1.
009
.25
».23
0.56
.0
37
.10
.008
.16
0.87
.0
58
.20
.009
.26
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 17
0w .&M S
§£ e
So
CMO
o
S
$
01 01
9o
fc
*
a
Sf Oss
O
sS_2
£
0
CO
6
sos
p?B
Q
I-§
o
"O
d
c0
§V
o0
CD
3tive hot springs,
an Isidro.
03 2"S
r.i£3S SH*» o
sS§s 2«03 n£003 '-I
O
8
?0W
X-55-2958
O
S
_xe
ow
5
3 8 g §o
3 8 o
1O 1O S « i-l OO O O
0
1 s 1 1o
1 5! S 10
^
0 <M S 0 O i-l O O
0 S 0 0
d
0 *< 10 10
1 I | I03 O O O 3OOO
o3 a ^f -j.
cp © 'C co *C ^ *C *3 t-i -»3 S ^3 ^a ^
"S E« « §«
sl fill II*° » >o-5'o So
l||l|iilo «°8°^ 0
<j m o« S5 15 S3J^ S J^ Sfc ^ ^ iz;
->i m DS oo oo oo poo
<N S S S
g O i-l CM CO CO CO
>>
|3.3g
£
CO OS "O CO
O i-l
CO t~
O i-i
S 3
O CD
0 -H
1 1
S S
1O -^
aring sandstone; property, Grants
« 0 9o
Jg.S o 3o
2 S .00 03 03 <
3
1C OO
?§ s
i «01 01
CO * CO CO
^< go ^a §< 8
3
10 10 o odo''
id CJ
d o
M CO §t>. i-l
N O Od rt
OJ CO CO N O Od od
m i-i oo
0 t;
00 Q CM Oesi « o ro
OSS! ^ « N00 r* O rH
O 1Q
rt Tt. -«. <N
'aring sandstone;
flotation Co.
og; Black Point- mple 36); 2 to 3 ft ample 36); 4 to 6 ft
^_- s-x ^
?a ^ ® bo o^ *&£H .^~" r^j
S||l§ 1,1?^ d? ^ tab 0 ti
Jllflsp3 O PH W
« <j m o^ ^ S ^
iiils « i sCO OO TO CO
18 CONTRIBUTIONS TO GEOCHEMISTRY
i ^
i 1a -i3 *3 a> o1) »
ii, m
>i
9
g»
?A
5aijJs>
§^
5, fe123>
%^
3§» jas AS 3 PS: o s0o0 35
|
: i
5 T2 § A w-
3. 1S 13 co a u Qi M
>3
^S A
5 1; "a* E aj33 1H -S
1i-:a "2
£ s tx
1M1ftl1Q»
«
iE^
s"cbP4
g8aEH
^_
&CB
§ 9 a
»0*
6^
7 " 1 g Ss Jg 93 Li §S*§ 1* 1
* t~ "*<o w 10 co o 't-:
rH
S So SO ' JH
^5 >o coo >oo t-
s»O "SO W CO
° '§
t~ rt 00
d '^ '
"*l Ot» WO> »O M U3
" '^
t- coco 10o '-o
N ,-HTtl <*!
tis'l i-s °.i
leistocene gravel (same location as sam 36); 2- to 3-in. layer of mineralized gra overlying scours in Chinle formati sample is mineralized cement and sma
gravel particles,
re sample; Jack Daniels No. 3 claim_ . yritic carbonacous log, unoxidiz
Huskon No. 22 mine,
re sandstone; Shinarump member Chinle formation; Kachina No. 1 cla:
PH OPn O
P «N P5T)« Cfl O) t*«
0 Q.-4 g
o So o
M «S S
S 33 9
V
0 ' cd
!S °CN i-H
C4 ^* IA * .-HO
O ' *»
CO «»-l I-H
MO" dj
ll LSI,
il tf 3o S >
t ?o oEH £HP3 f?
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 19
a 6 s §
on co o
ci
i s 2 3! 3 S 32CO *H
g-s
-
Is*;Sofe
8«-9°^ ^ ?at>"JH fl*l a
« _i n M r< *» 2 wfgrj^ii §^ § « a ® « « ®
i'S*B"Sl| fi
|S| 3si I§ls f?^l
II KlilSScriBlIJii.'ls!*>:§12fiil85|llg^
?-*J -^2 rtr
0
'
S.S (
00
6 t- CT>T1 T1e- ^ Art M W
20 CONTRIBUTIONS TO GEOCHEMISTRY
T!<D
fl4^
fi
I'S,s00
>
1tQ§>
Ss
I"
SM
lium-series disequilibrium analyses <
e-
1
H
W
H
3
o*3
o>
sft
Pn
£%
«So>
i
cs1IE |P
oIz;^ "3
>>
5£5Ki-l
Sa to
1
O
PH
S
M
iPH
1^
^
P o>
9 ft'§«
iz;
Iz;
owa
e
1
llS 4S 1B <3UTA
San Juan County (£
O O Ol rH t- 00
rH rH 00 * CO
10 rH tO SO
i t i t G5 Tf< COi-l i-l i-l i-l
rH *H O IO SO i-l W i-l *H
SO
O TO OS O >H IQ
<N rH C5 ' I-l I-l i-l IN i-l i-l
so to
a - a ' jj aI I *
1 I Ii i i
So JJ i-i co w M
i-l rH i-l i-l
Oi |Q C4 l» i-l O O
<N rH C3 * CO »0 rH O$ i-H i-H
* TH * CO * *
TH
SULFIDE ZONE ContinuedChip sample, altered lower sandstone; near floor at station 0, 15 ft south of station M.
Chip sample, lower siltstone; near floor at
station P, 70 ft south of station O.
Chip sample, pitchblende lens; between sandstone beds, north wall at station R,
25 ft west of station P.
Thin-bedded siltstone; abundant jarosite and limonite along fractures; 1.2-ft chan nel nearest floor of station V, 140 ft south
of station R.
Pitchblende seam at base of gray siltstone bed; grab sample near floor of station BQ,
50 ft south of station R.
Silty sandstone highly impregnated and replaced by yellow sulfides; 0.2-ft chan nel, 2.7 ft above floor at station 9, 310 ft
south of station BQ.
S> S> SO * O
^ $f f 0 00
M M W tf « «
t>- t- m So oo o
sees s 8
yfl?
aGO
i§
a
1e
San Juan County (
CM CO CO
O ' i-i
o S e§O -!
O CO ONI-I CO »OOO
O -H
o -^ us oo0 ' -i
S " 8O i-l
s % s§0 rH
(M r-t SOT*
0 ' I-i °
CO * TtlTH
Hyalite opal in sandstone from near base of Shinarump member of the Chinle formation; 10 ft from ore at Skyline mine, Monument Valley NWM, sec. 26, T. 43
S., R. 15 E., Salt Lake meridian.
Uranium-bearing sandstone from Deer
Flat,
.--.do... . ......._....-...-. .......... Mineralized carbonaceous material from
Hideout mine.
01
O 1 t CO
1 £?£?*""» U5 M M<j
s is is
co <£ co t*
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 21
±J
nab Cou
^
CM O
O
o *oCM O
o
3 10
* OOin O
8 io
s; s0 0
o
T)t
CO «
o
* Ttl
03 3
a 0
zs sandstone; Got
s Range.
?fr<
us usT I
O OOQ OQ
X O O
01 S
S S
xeaas%
fe 3o
5! So
to to00 10
0
§ §o
3 §8_;
K So
H >H
*" m ._S0} f* 0)
tillM rJ* fl Q.
terial; 0.5-ft chip 3tor mine, 80-ft lev
district,
nd mineralized m ample from Pro rale, Durkee distric
a t||.&o! S£fi!-S§ > &
CO
to to
s g8 00
K £
§H 5
oo
a«2
1Sa
.a
E-1
S"« o
1 *
1 5
H -S
l!5fe 0 ft
||
5
a
nnel on the south w
303
1o>
s"aQ
.H
|
1o>
£
* 00 1M 2 SrH r-l 1M O O O
O >H
O >-l 00 O O O
O
T-I Ol CO O O O
O iH
G5 00 CO CO T-H OT-l T-( 1O O O O
0 rH
OO O O> O ^
o J ° *
rH CO CO 0> T)t
o o to cS S oO ' i-i
i i co o o csO >H
TP TP rt CO CO CO
1 s 2 * « |1 S 1 * 1 »§3 1 « 1 3 |& §§"§§*
H 2 2 H o SO " O ^ w« g -a s -a 3_. N <B Trt ® ^5)K "C ,s S .3 a .S S 2 3 § 8 . S 2 SoS? 1 ^Sg -fl q-Og a 43 H° s Hgm-3 &«.«. . K ~hfi3®"- C^ CD .CD ® 73 CD CD
I'll I^plslf O H ^ CDT3 . _"nn P*CJ STJi»
«lgft«fi|2|J|SCQ OQ OQ OQ rt ft
OOOOgOO O O O g g
CO CO M CO « »S S « ?5 ^ S
8 SI 8 8 S3CO CO CJJ CO CO CO
S? w N ?3 ?5 ?5
s e E: e e 8
1gS>
1Is
J£
01 0 S
O 00 CO
S 0 CO
0 t-^ *
cU * 55O CO US
s * §o o us
a>
o t~ 06
*H CO i t to <-H O
o
t~CO to us
O * N
1-1 * **
K
c5 "3 *!3 *S ^
o ^. ^.^I'l| £ £ Ju-,2 §
I ll'lsli?I*Ma^-gj||a| go; a 5 gs * ®
M O O
u, S .
P5 " 'H, <J fe
SBi^ft ^ toS N 04
iH O) COoo oo oo
22 CONTRIBUTIONS TO GEOCHEMISTRY
T!
C
1
00
&> 1u
'e
< R. eS3
-o
&s«
%00-2> 'wCeS
ries disequilibriu
00
Se
j.
w
H
^j
1%<o *»
gPH
PH
i xjm r )
A ^i1
o"a
!p
ofc asPH
1
"o303
CO
1
PH
1
S
P3
i
fr
iPH
1
t>
o
tjCI,fcl *i
5
3
1
|
"g %
l!g i9 >
§ fcS -«2^Ej
P3
Ita
§ t^ CD O O
<3
-H <N § rt .H Oc>
s s So
S 83 1ei
CM o cq
o
i-l CM COO O »-H
us « ooS o o
* ^1 rt
! ! 5rH ,2 *M^
oote feg "SlN^CM 0^
iceous sandstone; Cro sec. U, T. 28 N., n. 9 ined sandstone; Croc sec. 24, T. 28 N., R. 8 ined conglomerate; BWM sec. 16, T. 28
%!|!|o ft ft
ft? ? ? f000pj pj pj
IIICM CM CM
Ttf 10 tO00 00 00
01m
0
t~oo oo
CO
o
SIH
iCM
<N
TO
CMGO O CO OTO
^
oo 8
rH TP
1 *»1O f-i
CD S . "^ *^§ M CM g -g g2
"m g g J3 g q* .
IS El'-S^
"S S "03 2 Q 3 CD
"^ ^jfe CM CD *3*JH w
Q o3 OJgiS*3 otCXj£§
3^ ^"
CM
tg tfe EH
feCO »O M "°CM t>-
lr~ oooo 06
B
o
O
gg |^
S t^ 0
c^ oo
rt
CM SCM'
gCM
O O
^s °-
^ *
« IIW . §a °° ycS'S-2
ne, Fort Union forma , sec. 3, T. 42 N., R. d white coarse-grain Fort Union forma Basin, near Kaycee.
lifiido 3*"
. S1C »H -I .1
1 t»
S E-1
Q 00
OS Ooo S
RADIOACTIVE DISEQUILIBRIUM OP THE URANIUM SERIES 23
Uraniferous breceiated vein material from bottom of a 35-ft deep inclined shaft in Precambrian granite and schist; Potter lease. SWJtfNWJi, sec. 23, T. 31 N., R.
C<l OCO 0O .-i
o ISO i-i
s s
nous woody sandstone from environment of Wasatch forma
. 4, T. 46 N., R. 74 W.
f J£-in. band of carnotite-type min timately associated with pyrite; ng a 1-ft thick seam of coal in the formation; Triangle claims, sec.
N., R. 73 W.
se ferru idized e n, sec. 4 ple of J£- l intim overlying
Wasatch f 28, T. 41
e oxidiz tion, s Sample ral i verly Wasat
C
"aP
£
|
P,o
o
o
id
3
TJ*
4> *jgj 035^'
£*-
Pyritic vein material from fissu Preeambrian granite of the No mie Range; sec. 27, T. 28 N., R
1£fe
1S
e| O
|d
1Ol
S t~»H OO ritcooo
o
i %$%0
I 95$
1 ^ss§O i-l
I
I
s §lso
rH TUTH^t
D
.a '3
Sandstone from Homestake Mi northwest of Devils Tower.
.do ................. ..... ..
do---. - - ..do .... . .....
1 SS2to fnfnfc
IIIIO tO b-00 G> O> OS O>
?fIIs 3
t.S
00
3 ".
>o
sCO
51
*53
*
^org.0 3 Ma|
Tyuyamunite from breccia zone Madison limestone; Pryor Mi
Big Pryor Mountain.
Ǥ
1CO
24 CONTRIBUTIONS TO GEOCHEMISTRY
T!
p)°43
§Q
I''S
S00
^
' S
1Je|g
5,<u
Ss
13irrange
00
fieg: 3»or-2
g.
00^m-series
^
\<N*
h-lpqH
"S SS<B
ag
PH
«
fePH
o>
gS
g"Si1'§Q
Field No.
fcoh
S"S
o>"3
CO
1
0
£
S
0
EH
MPH
f)EH
P
o>
s& ^«
^
0
Ke "e e SANA C
niels Coi
O
CO
8o
gd
1o
«
d
0od
"*
^JB
PP
MBS 174
t-oS?5
|
g§
I
aa
Sd
01-1
0CM
oi
go o'
§d
T*
CD
§
a
pq
a
o>3oCM
0
<
«
2^U5TX^CO
co
coco
*
^.co^
^^
«s
00
83
%4?o 3
Idorado pi ..do. __
W
IO *Q
1 11-5 1-5
§ rH
OopCM 55
si
< ^
M o" aQ w
M
d
o'H
3CM
^
co
Sco
CM *'
O>
"
a
1<8
S43«2o
i
aarbonaceot
o
GND-95A
CO
$S?CM
S
e
lings Coi
N
g
*t>-1-1
§rt
§""*
d
SorH
0
-
>o
"O*
Sfe
^a'3."
^2O ^^oi
ark-brown T. 13 N., ]
Q
So
CMO?SCM
1
e
aS?11
d
CMCO
51-1
«J
S^4
0o d
CDco d
«*
t-T
SSw^!
5? 3t^'03
CQ ^H
arbonaceoi 137 N., R.
D
13a
>*isSCM
S
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 25
O
to
o
so
or 00 COCO O
g
g 2° ^ o oo « CO 00
s s i si s -,CO O
s? e IM COCO C& W Ol 1-H
s
E -
s e I §§ s to «o °> 8
o
CO
o
0
COK §
ilii
o oo
£H
oO 1-H
i-< r-i to-* * i-iia *
Grab sample from ore zone in surface work ings; carnotite-type mineral in white sandstone host rock in Lakota sandstone; Damsite no. 1 claim, sec. 8, T. 8 S., R.
4E.
Sandstone with carnotite; Gould mine. sec.
12, T. 8 S., R. 3 E.
Radioactive barite _ ... .-.._ .... Ore pod in sandstone; sec. 11, T. 8 S., R.
3E.
Reaction zone around ore pod; same loca
tion as sample no. 110.
Clay; sec. 11, T. 8 S., R. 3 E.-. .... . Contact between clay and adjacent sand stone: same location as sample no. 112. Radioactive sandstone from Fall River
sandstone; light fraction; Red Canyon
CO
8
^S§ 10 IOIO <jg
3 "=> I I Ci' efl *j* -* FQco co coco O OQ FQP3 P3 P3P3 C3
CO 1OCC 00 U3C ill
Heavy fraction of same sandstone as sample
no. 114.
Opal concentrate from light fraction of same
sandstone as sample no. 114.
GG-lB-53 GG-1C-53
PQ g
iO CO
£ S3
2 g
00 CO
IO CO rH
co <N'
M *& co C3
So
0
Sio
8
^
£
8o
1-4
s83 a
o
"8
1
a
1
1
1rH
£
»!
1
3
enclosed in basal part of weathered yellow shale, Niobrara formation, SEH, sec. 28,
T. 36 N., R. 46 W.
26 CONTRIBUTIONS TO GEOCHEMISTRY
T3CD£3
1
1ar**
CO
&' 2
5.0
113s
rs<»
1*300
00
-5
«s
Ss~^o ea
"ea
g.§ 00<u*e<x>00
s"Ss
(§n 4H
"S
f3,"3
&
I
.afil
CD
c' £
§ c%cc
z^
£
c
ca
tO a(.
a "f
or.
1rt
a£1
«
§1P3
g
8
1
I
0
§ ©p,
»
.*
6
^M i*ig IH g
fe ||o
>O 5 CO
o
s ® §o
b* »o O
CO
1O CD O CO "~1
§ 00 SCN
oo
1-4 *O
cs
*4< ^ 10
.£f S . -9 t<
£|S g 8.
'i"S fe1 §"S 3 aT "o *
o ca g *S "
O § & 2 °aS"3 1 §a-fc® ft«°a o-g.2 . OTCT t>,olii^l:-^llg^S-il
» «§a8M rt-g^ rgg^S|l-Sjz:|ll§ S o W
<j PQrj O CO
§ 8 c^
Cl Q ft
<j pq
i 1 1a ss
K§O
io
oo oo
so o
oo
CD
ooo
oo
Tj.
aoas11io o
i a .Chattanooga Ridge, Tem
CM
Os
1§
*% 1o ia J
coV
CO
o
00CD
CO
1& s a O 3 »«Oa'SO °3°PQ°S 5* 2 mWater precipi tains consid
1^FQ
1
B
V
RADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 27
S c5
-H S1-1 o b* *oo i-i oi
* s §
53 S o o>
kO Jfi t- (-4
o w V V V V
1-1 1-T
^ o 8 8 ^ -c o
2 3 -! o»
CO 0 0 CO
Banded vesicular limestone, Arbuckle group; 2,529- to 2,530-ft depth, Magnolia-
Anderson no. 7, Augusta Field.
Dense vesicular limestone, Kansas City group; 2,027- to 2,037-ft depth; South
Anderson no. 1, Augusta Field.
Pipe scale from gas-well pipeline, Simpson formation SWH sec. 27, T. 9 S., R. 4 E. Scale collected from scrap pipe... __ ~ _
PH PH P-< j£
1 1 II§ § § S
3 t0 g3 0 0
T-t CO i-H i-l OiO O 00 OO
i § is § & sO i I
0 CO §0 1 » co«, « « m
<N O
N 3 -* CO
g ^ is 1 - c,^ V VV V V V
oo o o o co co
"= V V^ " '
eo ko ON o * i>1-4 CO IN CM
CO CO COCO CO CO CO
Filter cake from no. 2 tank, Cities Service,
Avant Unit.
Sulfate scale from water trough, Avant 1-S
well.
Ferrifloc from waste-water pit, Avant Unit- Fresh scale from outlet valve on Avant
Unit 1-S well.
Freshly precipitated ferrifloc from lime-
ferrifloc precipitate, Avant Unit.
Sand used for road ballast, previously used for oil-field filter sand, sec. 24, T. 24 N.,
R. 11 E.
Concretionary limonite and BaSO« from salt-water drainage ditch grading from
New Boston Pool.
CO t- 1-4CM CO
f f ff j* S S
S jo c»o 1-1 eg co00 00 OO C^ OS Oi O
CM CO ** kO CO t>- OO
0
o
s
CO
o
1-4
CO
Is& . M-J
=§ -o ra*.§2&a"<Q CQ gxfH
&
II C-3FQ
CO
tw
Is
lisa Cou
H
TAB
LE 2
. U
rani
um-s
erie
s di
sequ
ilib
rium
ana
lyse
s ar
rang
ed b
y ge
ogra
phic
al l
ocat
ion
of t
he s
am
ple
s C
onti
nued
TE
XA
S
Mid
land
Cou
nty
Kar
nes
Cou
nty
to 00
Sam
ple
No.
Lab
orat
ory
No.
Fiel
d N
o.D
escr
iptio
n an
d lo
catio
nD
is
equi
lib
rium
ty
pe
Perc
ent
eUU
Th2
32
Perc
ent e
quiv
alen
t
Pa23
iTh
M?
Rasz
sRn
222
Pbsio
Baa
"
141
2291
22E
T-1
10er
y, F
olso
m c
ultu
re.
20.
005
0.01
30.
0043
0.00
230.
001
3i
. 001
30.
001
0. 0
006
142
143
144
145
GX
-56-
45
GX
-55-
1258
GX
-55-
1272
GX
-55-
1277
56-1
PF
F-5
5-11
PF
F-5
5-23
PF
F-5
5-30
ium
min
eral
s; n
orth
tre
nch,
sou
th L
yssy
or
e bo
dy.
Soil
dire
ctly
ove
r sa
mpl
e 14
5, D
r.
Boz
ole
ase.
Mar
vin
Hac
bene
y ra
nch,
nor
thea
st
base
of T
ordi
lla H
ill.
Bla
ck s
ands
tone
; Dr.
Boz
o le
ase;
sou
thw
est
of n
os.
143
and
145.
leas
e.
1 4
lor
4 1
1.9 .41
.29
1.4
4.35 .65
.57
1.93
3.20 .66
.71
1.87
2.77 .96
.55
1.58
0.49 .76
.47
1.70
0.29 .24
.11
.97
0.33 .25
.10
.76
Duv
al C
ount
y
14fi
147
2280
87
2280
88
F-11
262
F-11
263
Whi
te
fria
ble
tuff
, C
ontin
enta
l O
il C
o.le
ase.
One
-foo
t ch
anne
l in
car
bona
ceou
s lig
nitic
mat
eria
l; A
rans
as E
xplo
ratio
n le
ase,
nor
th
Duv
al C
ount
y.
Sam
ple
is fr
om D
ubos
em
embe
r of
Jac
kson
for
mat
ion,
ove
rlies
med
ium
to f
ine-
grai
ned
fria
ble
sand
ston
e.E
adio
activ
ity o
ccur
s in
low
er 6
in
to 1
ft
of li
gnite
mat
eria
l whe
rp it
ove
rlies
hig
hly
silic
ified
por
tion
of n
orm
ally
fria
ble
sand
st
one.
4 4
.062
.26
0.05
1
.075
1.9 .55
2.5 .62
1.5 .47
0.82 .32
1.0 .37
i Ind
epen
dent
Ea«
« an
alys
is p
erfo
rmed
by
J. R
. D
oole
y an
d D
. L.
Scha
efer
usi
ng th
e ra
don-
trai
n m
etho
d,* V
ery
low
.3 I
nsuf
fici
ent s
ampl
e,
KADIOACTIVE DISEQUILIBRIUM OF THE URANIUM SERIES 29
SUMMARY
Radioactive disequilibrium is a fairly complex phenomenon, and it is not an easy task to provide simple and straightforward explanations for the various daughter-product abundances. An approach through multiple hypotheses whose possible acceptance or rejection will be based on further interpretations provided by geological, geochemical, and chemical evidence will undoubtedly be necessary. The initial goal of this study was to investigate the complexity of disequilibrium and the distribution of its types. Unfortunately many of the early samples that were analyzed did not have adequate enough descriptions to permit more detailed interpretations.
Some of the many possible explanations of the causes of disequilib rium have been presented here although some of these may have to be revised when further evidence is available. Even without accept ance of an hypothesis, radioactive-disequilibrium studies provide important clues to the geological and geochemical history of deposits.
REFERENCES
Armburst, B. F., Jr., and Kuroda, P. K., 1956, On the isotopic constitution ofradium (Ra224/Ra228 and Ra228/Ra226) in petroleum brines: Am. Geophys.Union Trans., v. 37, no. 2, p. 216-220.
Barnes, J. W., Lang, E. J., and Potratz, H. A., 1956, Ratio of ionium to uraniumin coral limestone: Science, v. 124, p. 175-176.
Chlopin, U. G., and Vernadsky, V. I., 1932, Radium-und mesothoriumbaltigenaturliche gewasser [Radium and mesothorium content in natural waters]:Zeitschr. Elektrochemie, Band 38, nr. 8a, p. 528-530.
Bison, R. E., 1954, The chemistry of protactinum, in Seaborg, G. T., and Katz,J. J., eds., The actinide elements (Natl. Nuclear Energy Ser., Div. IV, v.14A): New York, McGraw-Hill Book Co., p. 117.
Gott, G. B., and Hill, J. W., 1953, Radioactivity in some oil fields of southeasternKansas: U. S. Geol. Survey Bull. 988-E, p. 69-122.
Koczy, F. F., 1954, Geochemical balance in the hydrosphere, in Faul, Henry, ed.,Nuclear geology: New York, John Wiley and Sons, Inc., p. 120-127.
Kuroda, P. K., 1955, On the isotopic constitution of radium (Ra^/Ra229) inuranium minerals and recent problems of geochronology: New York Acad.Sci. Annals, v. 62, art. 8, p. 177-208.
Phair, George, and Levine, Harry, 1953, Notes on the differential leaching ofuranium, radium, and lead from pitchblende in H2SO4 solutions: Econ.Geology, v. 48, p. 358-369.
Rosholt, J. N., Jr., 1954, Quantitative radiochemical method for the determinationof major sources of natural radioactivity in ores and minerals: Anal. Chem istry, v. 26, p. 1307-1311.
1957a, Patterns of disequilibrium in radioactive ores, in Dunning, J. R., and Prentice, B. R., eds., Advances in nuclear engineering, v. II, pt. 2: New York, Pergamon Press, p. 300-304.
1957b, Quantitative radiochemical methods for the determination of thesources of natural radioactivity: Anal. Chemistry, v. 29, p. 1398-1408.
30 CONTRIBUTIONS TO GEOCHEMISTRY
Rosholt, J. N., Jr., 1958, Radioactive disequilibrium studies as an aid in under standing the natural migration of uranium and its decay products: United Nations Internat. Conf. on the Peaceful Uses of Atomic Energy, 2d, Geneva, 1958, Proc., paper QIC 183, U. N. 772.
Schumb, W. C., Evans, R. D., and Hastings, J. L., 1939, The radioactive deter mination of protactinium in siliceous terrestrial and meteroric material: Am. Chem. Soc. Jour., v. 61, p. 3451-3455.
Senftle, F. E., Stieff, Lorin, Cuttitta, Frank, and Kuroda, P. K., 1957, Comparison of the isotopic abundance of U235 and U238 and the radium activity ratios in Colorado Plateau uranium ores: Geochimica et Cosmochimica Acta, v. 11, no. 3, p. 189-193.
Stern, T. W., and Stieff, L. R., 1959, Radium-uranium equilibrium and radium- uranium ages of some Colorado Plateau secondary minerals, in Garrels, R. M., and Larsen, E. P., 3d (compilers), Geochemistry and mineralogy of the Colorado Plateau uranium ores: U. S. Geol. Survey Prof. Paper 320.
Trites, A. F., Jr., and Chew, R. T., 1955, Geology of the Happy Jack mine, White Canyon area, San Juan County, Utah: U. S. Geol. Survey Bull. 1009-H, p. 238.
Urry, W. D., 1948, The radium content of varved clay and a possible age of the Hartford, Connecticut, deposits: Am. Jour. Sci., v. 246, p. 689-700.
Wendorf, Fred, Krieger, A. D., and Albritton, C. C., 1955, The midland discovery, a report on the Pleistocene human remains from Midland, Texas, with a description of the skull by T. D. Stewart: Austin, Texas, Univ. of Texas Press, 139 p.
Wildish, J. E., 1930, The origin of protactinium: Am. Chem. Soc. Jour., v. 52, p. 163-177.
O