Science in Christian Perspective
Non-Radiometric Data Relevant
to the Question of Age
DANIEL E. WONDERLY
Rt. 2, Box 9 Oakland, Maryland 21550
From: JASA 27
(December 1975): 145-152.
This paper was presented at the 1973 annual meeting of the ASA. The author was
formerly Head of the Biology Department at Grace College, Winona
Lake, Indiana.
Within the past twenty years several useful types of age-indicating data have become available. An abundance of objective research reports on these subjects can now be easily found in scientific journals and other publications. It is time for creationists to begin to make far more use of such reports than we have in the past. We have often failed to realize that these are very helpful in making estimates of the earth's age. The record of God's work in nature is far more complete, informative, and worthy of consideration than we have usually thought.
It is our purpose here to list some of the specific types of data
available, giving
a few selected bibliographic references for each type. These sources have been
carefully chosen with a view to their being sufficient to serve as at least a
"starter" for anyone wishing to pursue a given subject. Most of the
sources themselves also have good bibliographies, which will readily enable any
interested person to locate numerous additional articles on the subject. An effort has been made to choose
those articles
and monographs which consist primarily of the objective results of
research rather
than of theory. However, in the references in which evolutionary
theory may appear,
the presence of some theoretical material need not obscure the facts which were
obtained in the research. The reader should keep in mind that long periods of
time do not necessarily imply evolutionary development, and that all
of the types
of data which are listed below appear to be in keeping with the
historical account
of creation that we find in Genesis 1 and 2,
Most of the bibliographic entries are available at the geology
library of practically
any large university. Other materials can be obtained from the
geological societies
of major oil producing states, and by means of interlibrary loan. The addresses
of most of the geological societies are found in a special Directory
section near
the back of each issue of the American Association of Petroleum
Geologists Bulletin.
Many of the sources can be used and understood without an extensive background
in geology. This paper is basically a listing of types of data, rather than a
composite monograph. There is a separate bibliography for each
section. The reader
will thus be able to consider any one subject separately, and locate
the bibliographic
references for that subject easily.
Carbonate Deposits
Drilling records from the sedimentary carbonate deposits of the Great
Bahama Bank,
off the coast of Florida. This is a multilayered deposit of various
forms of limestone
and dolomite somewhat in excess of 14,500 feet in thickness. In the
deeper parts,
dolomites alternate with limestones, with evidence of erosion between
four major
cycles of deposition. Identifiable fossils were found to a depth of
at least 10,600
ft. Alternations between limestone and dolomites in this and similar formations
indicate at least a corresponding number of changes of environment
during deposition
and during the process of dolomite formation. (See below on dolomite formation
and on limestone formation.) Also, the unconformities, at the levels
where erosion
is revealed, must represent significant amounts of time.1
Ooids
The distribution and rates of formation of the small, spheroidal bodies known
as ooids, oolites, or ooliths. (The term oolite is more properly used of rocks
containing the individual ooids.) Most ooids are concentrically
laminated, around
a core of extraneous material such as a grain of sand, a small shell fragment,
or a recrystallized fecal pellet. This process of adding concrete layers (which
can be readily observed with a microscope) is accomplished by a slow accretion
of mineral which is extracted from the sea water on the beach where the ooids
are being formed. The present-day formation of carbonate ooids is observable on
numerous shores where shallow water carbonate deposition is taking
place. Oolitie
limestone, with ooids of various types, appears at numerous levels in the Great
Bahama Bank and in many other carbonate deposits.2
Sediments
The similarities between the order of deposition of present-day
marine sediments,
and the order found in deep subsurface sedimentary deposits in oil
fields. These
similiarities are now being used by oil research geologists for understanding
and predicting the arrangement of older deposits deep in the earth.
This research
also deals with paleoecological topics, such as the faunal
associations and ecological
succession found in ancient strata, and compares them to moderm faunal associations observed in shallow-water depositional environments. Even though
we cannot accept all the tenets of uniformitarianism, the close
similarities between
modern marine carbonate deposition and these ancient deposits demand
that we recognize
slow, natural deposition as accounting for many thick carbonate deposits in the
oil fields.3
Oceanic Sedimentation
The thickness and arrangement of the layers of carbonate and siliceous skeletal
remains found on the ocean floor, formed by the accumulation of the shells of
Foraminifera, Radiolaria, and other planktonic organisms. A comparision of the
thicknesses of such deposits with current rates of deposition of
these skeletons
in parts of the ocean floor where there is no evidence of rapid deposition or
recent disturbance is meaningful. Of special significance are the
pelagic sediments
found in isolated parts of the ocean, such as on the tops of certain seamounts
and abyssal hills, which are far enough from land masses that the
rate of deposition
is not appreciably affected by currents bringing sediments from those
land masses.4
Plant and Invertebrate Skeletons
Present-day burial and fossilization of calcareous plant and
invertebrate animal
skeletons in marine coastal environments, on the sea floor, and in
the subsurface
of modern reefs. It has sometimes been said that processes of fossilization are
not occurring today, but recent studies of marine coastal
environments have revealed
numerous cases of the current formation of fossils.5
Dolomite Formation
The rate of dolomite formation in modern marine environments, combined with a
study of ancient formations which exhibit alternating dolomite (dolostone) and
calcium carbonate (limestone) strata. In recent years the process of
natural dolomite
production has been observed and studied in several marine environments which
have the proper conditions for the necessary magnesium ions to be
extracted from
the sea water and deposited. There are many lines of very strong
evidence indicating
that practically all dolomites-both ancient and modernare formed by a process
of replacement of calcium carbonate particles in lime sediment or limerock. In
order for dolomitization of such sediment or rock to occur there must
be a ratio
of Mg and Ca ions in the water which will favor the formation of dolomite, and
there must be an extensive circulation of the water over the sediment
or through
pores in the rock. Because dolomization proceeds by ion exchange it
is of necessity
a slow process, and can not occur to any appreciable degree without extensive
circulation of water.6
Deposits of Evaporites
Multilayered deposits of the (water soluble) evaporites anhydrite and
salt, which
often not only alternate with each other, but also alternate with (relatively
insoluble) calcium carbonate layers. The Castile Formation of west
Texas and southeastern
New Mexico is one such deposit, the thickness being in excess of 2,000 feet in
some places, including approximately 200,000 calcium carbonate-anhydrite "couplet" layers. The nature of
these thin layers of anhydrite and of calcium carbonate definitely shows that
they were deposited by precipitation. It should he remembered that
these two substances
do not precipitate at the same degree of concentration of the sea
water. Calcium
carbonate begins to precipitate when the sea water has been evaporated to about
half the original volume, but the precipitation of anhydrite does not
begin until
a volume of about 19% has been reached.
Thus it is evident that a major change in the concentration of the
sea water took
place 200,000 times, with the concentration coming back each time to at least
very near the same value. Furthermore, each of the precipitation events had to
be accompanied by quiet water, for allowing the mineral to settle to the bottom
to form the thin, uniform layer that it did. (The areal extent of these layers
is many miles, with almost uniform thickness of any given layer maintained over
at least a distance of 18 miles.) These are processes which required
very considerable
amounts of time.
Another very significant evaporitc formation which shows conclusive
evidence that
it was formed slowly is that found in the Mediterranean Sea. Beneath
the Sea floor
in several areas core drillings have revealed repeating layers of
fossil-bearing
oceanic sediments interbedded with evaporite layers, showing that the
Mediterranean
dried up numerous times. Also, in the Balearic abyssal plain, west of Corsica
and Sardinia a "bulls-eye pattern" of evaporite deposition was found.
In this deposit, layers of CaCO3, CaS04, and NaC1 were found in the
normal order
of precipitation when evaporation of sea water occurs. There is good evidence
that this evaporite deposit is a few thousand feet in thickness.7
Deposits of Sandstone and Shale
Multilayered deposits of sandstone and shale. An example is found in
the Haymond
Formation in the Marathon region of Texas. There are approximately 15,000 thin
sandstone layers alternating with approximately the same number of contrasting
shale layers in this formation. The study of such a deposit requires
that we carefully
consider the length of time required for the clay particles, which formed each
layer of shale, to settle out of suspension. The clay particles which
form uniform
layers such as this are extremely small, thus settling slowly, and only when a
minimum of turbulence exists.8
Modem Coral Reefs
The thicknesses of modern coral reefs, as related to the growth rates
of reef-forming
organisms. The thickest deposit of this kind measured to date is that
of the Eniwetok
atoll, where the test drill penetrated 4,610 ft. of coral deposit in order to
reach the volcanic seamount on which the reef was built. A study of
such deposits
in the light of present-day coral growth rates cannot produce an
exact chronology
of the past, but will nevertheless be very meaningful. This is because of our
recognition of the stability of God's natural laws, including the
laws of nutrition,
respiration, and secretion in living organisms. According to detailed
and extensive
studies by A. G. Mayor (1924) on the growth rates of various genera of corals
in the Samoan Islands (in a tropical area where conditions are most
favorable
The record of God's work in nature is far more complete, informative and worthy
of consideration than we have usually thought.
for rapid growth), the fastest rate of upward growth of the reef surfaces was
only about 8 mm per year.9
Ancient Coral Reefs
Ancient coral reefs, such as the atolls found in the oil fields of
Canada, together
with the extensive deposits of evaporites and other minerals which frequently
cover them. This is a geographic area where the process of comparing
modem reefs
and other modern carbonate deposits with the ancient has yielded
spectacular results
in predicting the best drilling sites (cf. reference 3). Some of the
atoll reefs
in the Rainbow Lake area of Alberta, Canada, are 800 ft. in thickness
at the rim,
and are strikingly similar to the crescent-atolls of the present-day
Great Barrier
Reef of Australia. The Rainbow Lake reefs contain abundant massive growths of
colonial corals in situ, as well as crinoids, stromatoporoids, brachiopods, and
gastropods. Thus, these were genuine, wave-resistant reefs which grew
in ancient
times, when most of central North America was covered by relatively
shallow ocean
waters. The multiple layers of evaporites and other thick mineral
deposits which
cover these reefs give witness of the long periods of time since that
geological
period (the Devonian) 10
Coral Growth Bands
The growth bands exhibited by ancient and modern corals and mollusks,
which appear
to be an accurate indicator of the daily growth rates of these
organisms, as well
as of the number of days in the year at the time when the animal was living. It
has been known since the beginning of this century that the corallites of some
kinds of modern corals possess annual growth hands. Now, within the
last decade,
it has been learned that these corals possess two lesser orders of growth bands
or ridges between the annual rings, the one marking the growth
increments of synodical,
lunar months, the other the increments of daily growth. When certain
fossil corals
from the deeper strata, e.g., from Devonian rocks of New York and Ontario, are
examined, they are found to show growth bands very similar to those of modern
corals, except that the number is approximately 400 instead of 365, apparently
indicating that these corals lived at a time far enough back that
there were 400
days in the year, and consequently slightly less than 22 hours in the day. (The
calculations of astronomers have shown clearly that the rate of rotation of the
earth is decreasing, but that the period of the earth's revolution around the
sun has been essentially constant. Thus, in earlier times, though the absolute
length of the year was the same as now, the earth's rotation was more
rapid, making
the days shorter, and also affecting the number of lunar-and tidal-months in a
year.) The growth rings on the Devonian corals thus show that they
lived and grew
at a very early date; and the size of the rings shows that the growth rates of
these corals were not very different from the growth rates of modern corals. The
growth bands
which have been observed on certain ancient bivalve mollusk shells
are in essential
agreement with the findings in corals.11
Organic Banks
Various types of ancient carbonate organic banks, and cyclic deposits
which include
layers of definite, identifiable fossils. The larger of these banks are usually
spoken of as reefs in geologic literature. Examples are the famous
"Horseshoe
atoll" (or Scurry reef) of west Texas, the numerous Silurian
reefs of Indiana,
and the Capitan reef of west Texas and New Mexico. Organic banks
which are moundlike
in shape and enclosed in rock of a contrasting type, are usually
called bioherms,
though the terms reef and bioherin are often applicable to the same
structure.
Some of these organic banks are very large, lie at great depths, and
are components
of extensive, local stratigraphic columns. For example, the Capitan reef is 350
miles long, and 2,000 ft. thick in places; and the eastern half of it lies in
a large oil field, at a depth of some thousands of feet. Numerous alternating
layers (cyclic deposits) of evaporites make up an extensive part of
the formations
which cover it. This reef has numerous bryozoan colonies and other
fossils still
in growth position (in situ). Beneath the Capitan reef there are, in
some localities,
more than 15,000 feet of sedimentary rock. This rock consists of
numerous distinct
layers of limestone, dolomite, sandstone, shale, etc., alternating
with each other.
Most of these deep layers underlying the reef possess identifiable fossils.
Often an ancient organic bank will he associated with, or a part of, a group of
repeating depositional units called cyclothems. A cyclothem is a
series of sedimentary
layers which repeats itself in the stratigraphic record in a
particular locality.
Each eyclothem represents the depositional results of a series of
changing environments
in the ancient locality involved. The fact that several very similar cyclothems
sometimes exist in a local stratigraphie column, and that evaporite layers and
other environmental indicators frequently make up a part of each eyclothem, is
conclusive evidence that these are naturally formed series representing rather
large units of time. It is also significant that cyclothems contain
sub-cycles.
Calcareous algal, limestone banks and mounds are often found lying deep in the
strata of oil fields. These are of course a type of organic hank, having been
produced by calcium-secreting algae which are similar to the many
species of calcareous
algae which we have today. The fossilized remains of the algae in these banks
give every evidence of being in situ, and of having accumulated in a
manner similar
to the formation of algal deposits in modern tropical marine environments.
Recent extensive research has shed much light on the true nature of limestones
such as those found in the organic banks. The study of the various
types of organic
banks, together with a comparison of the carbonate depositional
processes in modem
marine environments, has shown that a very high percentage of the
limestone deposits
of the earth was formed by the gradual accumulations of calcareous animals and
plants rather than by inorganic processes. Even though diagenetic
change obliterates
many of the skeletons of these organisms, sufficient parts usually remain (with some of the
substrate material on which they were growing) so that we can be
sure, in at least
many cases, that they were preserved either at or near the place
where they grew.
Since most limerocks have large amounts of microscopically
identifiable particles,
it has been observed that the layers of major limestone deposits are
usually composed
of normal assemblages of grains and other characteristic particles. These are
frequently very similar to the assemblages found in modern carbonate
rock-forming
environments such as those of the Caribbean area and other parts of
the world.
Often the fossils found so abundantly in a given bed of limestone
make up a typical
marine faunal and floral community, and a significant percentage of
the delicately
articulated skeletons will be intact, showing that they were not
transported any
long distance. Also, the lack of signs of abrasion of certain carbonate grains,
such as fecal pellets, in the rock, and the lack of size sorting of the various
types of grains are further evidence that the limestone was formed in
situ without
extensive transport of the materials of which it is composed. One of the must
spectacular examples of evidence for the in situ formation of limestones, as a
result of the growth of organisms, is the rounded, laminated masses
of limestone
which are called stromatolites. Extensive study of very similar
structures being
formed today in some carbonate depositional environments has made
possible a detailed
analysis of the ancient stromatolites. (Each stromatolite is formed by a large
mass of algae growing in the water, and collecting layers of carbonate grains
on its gelatinous surface as the water sweeps over it.)
The presence of layers of shale between the layers of limestone in
many formations
has usually aided in the preservation of the skeletal material, and
in the identification
of the environments in which the limestone layers were accumulated.12
Stratigraphic Columns
Well logs and drilling cores from oil fields, which provide us with
the structure
and composition of entire, local stratigraphic columns. In the past we have too
often neglected to study the deeper parts of the local stratigraphic columns in
areas where we have focused attention upon a single geologic formation. There
are now available very complete records of the local columns in many geographic
areas in the literature of petroleum geology. For example, Hughes (1954) gives
the 16,705 ft. column of the Richardson and Bass No. 1 Harrison-Federal well,
in the Delaware Basin of southeast New Mexico, as a 167 inch printed column. By
devoting one inch to each 100 feet of well core he was able to show
the lithnlogy
of the entire well in considerable detail. Also included are the generic names
of some of the fossils, to a depth of 16,000 ft. Such records as this help make
possible a study of both the chemical and physical nature of the
contrasting layers
in the column, as well as of some of the types of animals and plants present at
the times of deposition. The availability of these well logs and drilling cores
makes it possible for interested persons to study the geologic record directly,
without having to depend on composite columns or abbreviated summaries.13
Distribution of Marine Fossils
The unequal distribution of marine fossils in limestone and other formations.
An example of this is the abundance of certain kinds of very dense,
thick-shelled
mollusks of Class Pelecypoda in the upper strata, but an absence of
the same types
in lower layers. Conversely, some of the less dense animals, e. g.,
numerous species
of arthropods of Class Trilobita, are abundant in lower strata but
are not found
in upper layers. Recent electron microscope studies of the chitin of trilobite
skeletons give evidence for a low density for these animals.
Similarly, many species
of the cephalopods, of Phylum Mollusca, though very buoyant due to
the air chambers
of their shells, are found only in the deeper strata of the earth, indicating
that they were buried before the formation of the Mesozoic and Cenozoic strata,
and that they became extinct before the Mesozoic and Cenozoic strata were laid
down. Thus, the unequal distribution of marine fossils is another indication of
the long history which these organisms have, and the theory of some
of the proponents
of "flood geology" which says that the unequal distribution
is largely
due to densities is shown to be erroneous.
Even the very fact that many types of fossils are abundant in only a
small percent
of the stratigraphic column in a given locality, but not found at all in other
parts of that column, should be a cause for much serious study. In such columns
a great many species which are present at the lower levels are not present in
the upper strata at that site, nor in the corresponding strata at other sites.
The prevalence of this condition calls for recognition of a long period of time
for the formation of the larger (thicker and more extensive)
stratigraphic columns.
14
Forest Deposits
The multiple forest deposits in Yellowstone National Park. The data collected
during the study made by Dorf and his associates, concerning the numerous types
of fossil vegetation and preserved foliage in the strata of Specimen Ridge and
Amethyst Mountain, have apparently not been used to any extent by creationist
writers. Whitcomb and Morris have tried to explain these forest
deposits by saying
the trees were floated into place during the Flood, forming a
semblance of successive
forests preserved in volcanic ash. The work of Dorf makes this theory
completely unacceptable.15
Sea-Floor Spreading
The present and past rates of sea-floor spreading as exhibited in the oceanic
ridges, and the thicknesses of pelagic sediments which lie upon the ocean floor
at various distances from the present mid-line of the ridges. The present rate
of sea-floor spreading along the Mid-Atlantic ridge is estimated to be only a
few centimeters per year. The fact that the sediments are thin near the center
line of the ridge, and become gradually thicker farther away from the ridge, on
each side, is an indication that the spreading has been practically continuous
and gradual for a long period of time. Also, the linear strips of igneous rock
which lie to the west of the ridge are practically identical to the linear strips extending along the east side. Thus, one side forms
a "mirror
image" of the other, with respect to the chemical and magnetic nature of
the parallel trends of igneous rock. This gives us much reason to believe that
each pair of corresponding strips was formed at approximately the
same time, from
the same mass of magna along the ridge, and that the slow spreading
of the floor
at the rift has resulted in their now being widely separated. The
above mentioned
symmetry along the Mid-Atlantic ridge has been carefully mapped, and
the two sides
correlated for a distance of about 125 miles out from the center of
the ridge.16
Magnetic Reversals
The geologic records of magnetic reversals in igneous bodies of rock (both on
the continents and in the ocean floors), and in sediment cores taken from the
ocean floor. A great many extensive rock masses of these types, which exhibit
an orderly series of reversals, have been discovered during the past ten years.
For example, there is a close agreement between the series of reversals found
in ancient lava flows of the Rocky Mountains and those in the
Atlantic sea-floor.
There are many strong evidences that most of these reversals which
are "frozen"
into the igneous rocks are separated from one another by at least hundreds of
thousands of years. 17
K-Ar "Clock"
Even though we are presenting here a list of types of non-radiometric
data, there
is one phase of radiometric dating which should be mentioned, because
it has apparently
gone unnoticed by a great many creationists.
The discovery that the potassium-argon "clock," in rocks
which effectively
retain radiogenie Ar40, is restarted whenever the rocks are heated
(or reheated)
to a temperature of 300° C., or more. Recent writers on this type of dating
state that all original argon is lost, when such heating of igneous
and metamorphic
rocks occurs. Thus when the amount of argon present is measured, only
the amount
produced in the rocks since they were last heated can be detected.
This characteristic
is often listed as a disadvantage, because this means that
potassium-argon dates
can give only the length of time since the rock mass was last cooled
to a temperature
below 3000 C. However, this feature is an advantage for those who are
interested
in determining how long it has been since igneous or metamorphic rock
masses were
in a heated condition.
Perhaps we should also mention that Dalrymple, Moore, and others
recently discovered
that some of the earlier potassium-argon dates obtained for igneous rocks which
had been formed in deep water were very incorrect (much too old).
Their research
showed that whenever lava is erupted into a deep-water environment,
the hydrostatic
pressure, and the rapid cooling caused by the cold water, causes excess Ar4' to
be "frozen" into the outer parts of the lava mass. Earlier, when this
principle was not known, numerous samples of marine volcanic basalt
were wrongly
dated. However, now that the scientific world has been alerted to
this principle,
only the potassium-argon dates from continental formations and from
samples taken
from
the interior of submarine masses of rock are considered
reliable.18
BIBLIOGRAPHY
lEwing, M., Worzel, J. L., et at., 1969, "Shipboard site
reports," Pt.
1 in Initial reports of the Deep Sea Drilling Project-vol. 1, Leg 1 of cruises
of Glomar Challenger: U.S. Govt. Printing Office, p. 10-317.
Goodell, H. C. and Garman, R. K., 1969, "Carbonate geochemistry
of Superior
deep test well, Andros Island, Bahamas": Am. Assoc. Petrol. Geologists
Bull.
vol. 53, p. 513-536, 7 Fig's., 1 Table.
2Bathurst, R. C. C., 1971, Developments in Sedimentology No. 12,
Carbonate Sediments
and their Diagenesis: Elsevier Pub. Co., 620 p. (Chapter 7,
"Growth of ooids, pisolites, and grapesfone")
Cloud, P. E., Jr., 1962, "Environment of calcium carbonate deposition west
of Andros Island, Bahamas": U.S. Geol. Sure. Profess. Paper no. 350, 138
p.
Donahue, J., 1969, "Genesis of colite and pisolite grains -An
energy index":
Jour. Sedimentary Petrology, vol. 39, p. 1399-1411.
Tiling, L. V., 1954, "Bahaman calcareous sands": Am. Assoc. Petrol.
Geologists Bull., vol. 38, p. 1.95.
Newell, N. D. Purdy, E. G., and Imbrie, J., 1960, "Bahamian
oohtie sand":
Jour. Geology, vol. 68, p. 481-497.
3Davies, D. K., Ethridge, F. C., and Berh, R. R., 1971,
"Recognition of harrier
environments": Am. Assoc. Petrol. Geologists Bull. vol. 55, p.
550.565.
Friedman, C, M., 1970. "The Bahamas and Southern
Florida-A model for carbonate deposition": Shale Shaker,
vol. 21, p. 4-17. (This is an especially helpful article, with a good
bibliography.
Shale Shaker is published by the Oklahoma City Geological Society, Inc., 1020
Cravens Building, Oklahoma City, 73102.)
_____ 1969, "Depositional environments in carbonate rocks-an introduction," in
Depositional Environments in Carbonate Rocks: Soc. Econ. Paleontologists and
Mineralogists, Spec.
Pub]. no. 14, p. 13.
_____ 1971, "Petroleum geology-criteria for recognition of
depositional environments
in carbonate rocks": McGraw-Hill Encyclopedia of Science and Technology,
3rd edition. McGraw-Hill Book Co.
Ladd, H. S., ed. 1957, Treatise on Marine Ecology and Paleoecology, Vol.
II., Paleoecology: Geol. Soc. Amer. Mem. 67, 1077 p.
Loman, S. W., 1949, "Sedimentary facies in Gulf coast": Am.
Assoc. Petrol.
Geologists Bull., vol. 33, p. 1939-1997. Natlaud, M. L., 1933,
"The temperature
and depth distribution of some recent and fossil Foraminifera in the Southern
California region": Bull. Scripps Inst. Oceanog., vol. 3, p. 225-230.
Purdy, E. G., 1964, "Sediments as substrates," in
Approaches to Paleoecology, Imbrie, J., and Newell, N., eds.:
John Wiley & Sons, p. 238-271.
Stanley, S. M., 1966, "Paieoecology and diagenesis of Key Largo limestone,
Florida": Amer. Assoc. Petrol. Geologists Bull., vol. 50, p.
1927-1947.
Walker, K. R., 1972, "Community ecology of the Middle Ordovician
Black River
Group of New York State": Geol. Soc. America Bull., vol. 83, p.
2499-2524.
Walton, W. R., 1964, "Recent foraminiferal ecology and paleoecology,"
in Approaches to Paleoecology, Imbrie, J., and Newell, N., eds.: John
Wiley and
Sons, p. 151-237.
4American Geological Institute, 1973, "Across the southern
Indian Ocean aboard the Giomar Challenger," Geotimes,
vol. 18, no. 3, p. 16-19.
Ewing, M., Ewing, J. I., and Taiwani, M., 1964, "Sediment distribution in
the oceans; the MidAtlantic Ridge":
Geol. Soc. America Bull., vol. 75, p. 17-36.
Hays, J. D., and Opdykc, N. D., 1967, "Antarctic Radiolana,
magnetic reversals,
and climatic change": Science, vol. 158, p. 1001-1011.
Maczen, B.C., MacGregor, I. D., et al, 1972, "Deep Sea drilling,
Leg 20": Geotimes, vol. 17, no. 4 (April 1972), p. 10-14.
Keen, M. J., 1968, An Introduction to Marine Geology: Pergamoo Press,
218 p. (Chapter
4, "Pelagic Sediments") Ninkovich, D., Opdyke, N., Heczen, B. C., and
Foster, J. H., 1966. "Paleomagnetic stratigraphy, rates of deposition and tephrachronology in North Pacific deepsea sediments":
Earth
& Planet Sci. Letters, vol. 1, p. 476 ft.
Opdyka, N. D., Glass, B. Hays, J. D., and Foster J., 1966, "Paleomagnetie
study of Antarctic deepsea caret": Science, vol. 154, p. 349-357.
Pessagno, E. A., Jr. 1969 Mesozoic planktonic Forminifera and Radtolaria,"
in Initial Reports of the Deep Sea Drilling Project, vol. 1, Leg 1 of cruises
of Glamor Challenger: U. S. Govt. Printing Office. p. 607-621.
Phillips, J.D., et. al., 1967, "Paleomagnetic stratigraphy and
micropaleontology
of three deep sea cores from the central north Atlantic Ocean": Earth and
Planetary Science Letters, vol. 4, p. 118 ff.
Riedel, W. R., 1963. "The preserved record-Paleontology
of pelagic sediments," in The Sea, vol. 3. The Earth Beneath the
Sea, p. 866-887, Hill, M. N., ed.: Interscienee, New York.
Rodgers, John, 1957, "The distribution of marine carbonate
sediments-a review,"
in Regional Aspects of Carbonate Deposition, a Symposium: Soc. of
Econ. Paleontologists
and Mineralogists, Spec. Pub. no. 5, p. 1-13.
Weser, 0. E., 1970 "Lithologic summary," in Initial Reports of the Deep Sea Drilling Project, vol. 5,
Leg 5 of cruises of
Glamar Challenger:
U.S. Govt. Printing Office, p. 569-620.
5Bathurst, R. C. C., 1971, Developments in Sedimentology No.
12, Carbonate Sediments and their Diagenesis: Elsevier Publishing Co., 620 p.
(Several chapters of this work describe processes of burial and chemical change
of skeletal remains in coastal environments.)
Belsrens, E. W., and Frishman S. A., 1971, "Stable carbon
isotopes in blue-green
algal mats": Jour. Geol., vol. 79, p. 94-100.
Emery, K. 0., Tracey, J. I., Jr., and Ladd, H. S., 1954, "Bikini
and nearby
atolls, Marshall Islands; Part 1, Geology": U. S. Geol. Surv.
Profess. Paper
no. 260A, 263 p.
Johnson, J. H., 1961, Limestone-building Algae and Algal Limestones: Colorado
School of Mines, 297 p.
Kendall, C. G., St. C., and Skipworth, P. A. d'E., 1968,
"Recent algal mats of a Persian gulf lagoon": Jour. Sed. Petrology, vol. 38, p. 1040-1058.
Scoffin, T. P., 1972, "Fossilization of Bermuda patch
reefs": Science,
vol. 178, p. 1280.1282.
6Atwood, D. K., and Bubb J. N., 1970, "Distribution of dolomite in a tidal
flat environment, Sugarloaf Key, Florida":
Jour. Geol., vol. 78, p. 499-505.
Blatt, H. B., Middleton, C., and Murray, R., 1972, Origin of Sedimentary
Rocks:
Prentice-Hall, 634 p.
Chiliogar, C. V., Bissell, H. J., and Wolf, K. H., 1967,
"Diagenesis of carbonate rocks," in Developments in
Sedimentology No. 8, Diagenesis in Sediments, Larsen G., and Chilinger, G. V.
eds.: Elsevier Pub. Co. p. 179-322 (Pages 287-298 deal with
diagenesis of dolomites).
Friedman, G. M., and Sanders, J. F., 1967, "Origin and
occurrence of dolostones,"
in Developments in Sedimentology No. 9. Carbonate Rocks, Chihngar, G.
V., Bissell,
H. J., and Fairbridgc, R. W., eds.: Elsevier Pub. Co., P. 267-348.
Ham, W. F., 1951, "Dolomite in the Arbuckle Limestone, Arbuckle Mountains,
Oklahoma": Geol. Soc. Am. Bull., vol. 62, p. 1446-1447.
Hayes, P. T., 1964, "Geology of the Guadalupe Mountains, New Mexico":
U. S. Geol. Sure. Profess. Paper no. 446, 69 p.
Jodry, R. L., 1969, "Growth and dolomitizatioo of Silurian
reefs, St. Clair
County, Michigan"; Am. Assoc.
Petrol. Geologists Bull., vol. 53, p. 957-981.
Maher, J. C., ed., 1960, Slratigraphic Cross Section of Paleozoic Rocks, West
Texas to Northern Montana: Am. Assoc. Petrol. Geologists, Cross
Section Publication
no. 2, 18 p., 6 plates (vertical section maps).
Murray, R. C., 1969, "Hydrology of South Bonaire, N. A.
-A rock selective cloinmitization model": Jour. Soc. Petrology, vol. 39,
p. 1007-1013.
Shinn, F. A., 1968, "Selective dolomitization of recent
sedimentary structures":
Jour. Soc. Petrology, vol. 38, p. 612-616.
_____ Ginsburg, R. N., and Lloyd, R. M., 1965,
"Recent supratidal dolomite from Andros Island, Bahamas," in Dolomitization and Limestone
Diagenesis-A
Symposium, Pray, L. C., and Murray, B. C., eds.: Soc. Econ. Paleontologists and
Mineralogists, Spec. Pub. no. 13. p. 112-123.
_____ and Lloyd, R. M., 1969, "Anatomy of a modern carbonate tidal
flat, Andros
Island, Bahamas": Jour. Soc. Petrology, vol. 39, p. 1202-1228.
7Anderson, H. Y., Dean, W. E., Jr., Kirkland, D. W., and Snider, H. I., 1972,
"Permian Castile varved evaporite sequence, West Texas and New
Mexico":
Geol. Soc. Am. Bull., vol. 83, p. 5986.
Dean, W. E., Jr., 1967, Petrologic and Geochemical Variations in the
Permian Castile
Voreed Anhydrite, Delaware Basin, Texas, and New Mexico, Ph. D.
Thesis: University
of New Mexico, Albuquerque, N. M., 326 p.
Fuller, J. G. C. M., and Porter, J. W., 1969, "Evaporite formations with
petroleum reservoirs in Devonian and Mississippian of Alberta,
Saskatchewan, and
North Dakota": Am. Assoc. Petrol. Geologists Bull., vol. 53, p. 909-926.
(There are also twelve other articles on evaporites and evaporite deposits in
this April, 1969 issue of the Bulletin.)
Hsu, K. J., 1972, "When the Mediterranean dried up,"
Scientific American,
vol. 227, no. 6 (Dec. 1972), p. 27-36.
Kirkland, D. W., and Anderson, H. V., 1970, "Microfolding in the Castile
and Todilto evaporites, Texas and New Mexico": Geol. Soc. Am. Bull., vol.
81, p. 3259-3282.
Ryan, W. B. F., H. O, K. J., et al, 1973, Initial Reports of
the Deep Sea Drilling Project, vol. 13. pt. 1 and pt. 2: Washington
(U. S. Govt.
Printing Office), 1447 p. (NS 1.2: D36/2/v. 13/pt. 1, pt. 2.)
Smith, R., ed., 1967, Stratigrophic Gross Section of Paleozoic Rocks, Oklahoma to
Saskatchewan: Am. Assoc. Petrol.
Geologists, Gross Section
Publication no. 5, 23 p., 6 plates (vertical section maps).
8Dzulynski, S., and Walton, E. K., 1965, Developments in
Sedimentology No. 7, Sedimentary Features of Flyseh and Greywackes: Elsevier
Publishing Co., 274 p.
Grim, R. E., 1962, Applied Clay Mineralogy: McGrawHill Book Co., 422 p.
Lajoie, J., ed., 1970, Flysch Sedimentology in America: The Geological Assoc. of Canada, Spec. no. 7, 272 p.
Millot, G., 1970, Geology of Clays; Weathering, Sedimentology, and
Geochemistry, Faraud, W. H., and Paquet. H., trs.: Springer-Verlag,
Inc., 429 p.
9Edmondson, C. H., 1929, "Growth of Hawaiian corals":
Bernice P. Bishop
Museum Bulletin, no. 58 (Honolulu, Hawaii). 38 p.
Emery, K. 0., Traccy, J. I., Jr., and Ladd, H. S., 1954, "Bikini
and nearby
atolls, Marshall Islands: Part 1, Geology": U. S. Geol. Surv.
Profess. Paper
no. 260A, 263 p.
Hoffmeister, J. E., 1964, "Growth rate estimates of a
Pleistocene coral reef
in Florida": Geol. Soc. America Bull., vol. 75, p. 353-358.
Ladd, H. S., and Schlanger, 5. 0., 1960,"Bikini and nearby
atolls, Marshall
Islands, drilling operations on Eniwetuk atoll": U.S. Geol. Sure. Profess.
Paper no. 260Y, 36 p.
_____ 1961, "Reef-building": Science, vol. 134, p. 703-715.
Mayor, A. C., 1924, "Growth rate of Samoan corals," in
Papers from the
Department of Marine Biology of the Carnegie Institute of Washington,
v. 19: Carnegie
Inst. Pub, no. 340, p. 51-72.
10Barss, D. L., Copland, A. B., and Ritchie, W. D., 1970, "Geology of the
Middle Devonian reefs, Rainbow area, Alberta, Canada": in Geology of Giant
Petroleum Fields, Halbouty, M. T., ed., Am. Assoc. Petrol. Geologists
Memoir 14,
p. 19-49.
Hriskevich, M. E., 1970, "Middle Devonian reef production, Rainbow area,
Alberta, Canada": Asn. Assoc. Petrol.
Geologists Bull., vol. 54, p. 2260-2281.
Laugtun, J. H., and Chin, G. E., 1968, "Rainbow Member facies and related
reservoir properties, Rainbow Lake, Alberta": Am. Assoc. Petrol.
Geologists Bull., vol. 52, p.
1925-1955.
11Berry, W. B. N., and Barker, R. M., 1968, "Fossil bivalve
shells indicate
longer month and year in Cretaceous than present": Nature, vol.
217, p. 938-939.
Mazzullo, S. 5., 1971, "Length of the year during the Silurian
and Devonian
Periods-New values": Geol. Soc. America Bull., vol. 82, p.
1085-1086. Runcorn,
S. K., 1966, "Corals as palcontological clocks": Scientific American,
vol. 215, no. 4 (Oct. 1966), p. 26-33. Scrutton, C. T., 1965, "Periodicity
in Devonian coral growth: Paleontology, vol. 7, p. 552-558.
12Achauer, C. W.,
1969 "Origin of Capitan Formation, Guadalupe Mountains, New
Mexico and Texas":
Am. Assoc. Petrol. Geologists Bull., vol. 53, no. 11, p. 2314-2323.
Blatt, H.
B., et al. (See section No. 6 above).
Duff, P. MeL. D., Hallam, A., and Walton,
E. K., 1967, Developments in Sedimentology No. 10, Cyclic Sedimentation:
Elsevier
Pub, Co., 280 p.
Frost, J. G., 1968, "Algal banks of the Dennis Limestone
(Pennsylvanian) of eastern Kansas": Unpub. Ph.D. dissort.,
Kansas University.
Harbaugh, 5. W., 1962, "Geologic guide to Pennsylvanian marine
banks, southeast
Kansas," in Geoeconomics of the Pennsylvanian Marine Bunks in
Southeast Kansas:
Kansas Geol. Soc. 27th Fld. Conf. Guidebook, p. 13-67.
Harbaugh, 5. W., 1964,
"Significance of marine banks in southeastern Kansas in
interpreting cyclic
Pennsylvanian sediments": Kansas Geol. Survey Bull no. 169,
Johnson, J. H.,
1961, Limestone-building Algae and Algal Limestones: Colorado School of Mines,
297 p.
Heckol, P. H., and Cocke, J. M., 1969, "Phylloid
algalmound complexes
in out-cropping upper Pennsylvanian rocks of mid-continent": Am.
Assoc. Petrol.
Geologists Bull., vol. 53, p. 1058-1074.
Klement, Karl W., 1969, "Phylloid
algal banks (abs.)": Am. Assoc. Petrol. Geologists Bull., vol.
53, p. 207-208.
Merriam, D. F., and Sneath, P. H. A., 1967, "Comparison of
cyclic rock sequences,
using crossassociation": in Essays in Paleontology and Stratigraphy, Dept
of Geol., U. of Kansas Spec. Pub. no. 2, p. 523-538.
Moore, H. C.,
1962, "Geological
understanding of cyclic sedimentation represented by Pennsylvanian and Permian
rocks of northern Midcontinont region," in Geoecononsics of the
Pennsylvanian
Marine Banks in Southeast Kansas: Kansas Geol. Soc. 27th FId. Conf. Guidebook,
p. 91-100.
Myers, D. A., Stafford, P. T., and Buruside, H. J., 1956,
North "Geology of the Late Paleozoic Hureshoe atoll in West
Paper Texas":
University of Texas Publication no. 5607, Bureau of Economic Geology,
113, p.
Newell, N. D., et al, 1953, The Permian Reef Complex of the Guadalupe Mountains
Region, Texas and New Mexico: W. H. Freeman and Co., 236 p.
Peterson,
J. A., and
Hite, H. 5., 1969, "Pennsylvanian evaporate-carbonate cycles and
their relation
to petroleum occurrence, southern Rocky Mountains": Ann. Assoc.
Petrol. Geologists
Bull. vol. 53, p. 884-908.
Stafford, P. T., 1959, "Geology of part of the
Horseshoe atoll in Scurry and Kent counties, Texas": U. S. Geol. Surv. Profess.
Paper no. 315-A., 20 p.
Vest, E. L., Jr., 1970, "0il fields of
PennsylvanianPermian
Horseshoe atoll, West Texas": in Geology of Giant Petroleum Fields,
Halbouty,
M. T., ed., Ann. Assoc. Petrol. Geologists Memoir 14, p. 185-203.
Wray, J. L.,
1962, "Pennsylvanian algal banks, Sacramento Mountains. New Mexico,"
in Geoeconomics of the Pennsylvanian Marine Banks in Southeast Kansas: Kansas
Geol. Soc. 27th Fld. Cant. Guidebook, p. 129-133.
Logan, B. W., Rezak, H., and Ginsburg, H. N,, 1964, "Classification and environmental significance of
algal stromatolites": Jour. Geology, vol. 72, p. 68-83.
13Am.
Assoc. Petrol.
Geologists, 1960 to 1968, the "Stratigraphic Cross Section" Series.
(See Maher, 5. C., ed., 1960, in section 6 above, and Smith, H., ed., 1967, in
section 7 above.)
Goodell, H. C., and Garmau, R. K., 1969.
Hughes, P. W., 1954,
"New Mexico's deepest oil test": in Guidebook of
Southeastern New Mexico
(Fifth Field Conference), New Mexico Cool. Soc., p. 124130.
Roswell Geological
Society, 1958, "North-South Stratigraphic Cross Section Delaware Basin to
Northwest Shelf,
Southeastern New Mexico" (a vertical section map of an oil
producing area).
West Texas Geological Society, 1963, "Cross Section Through Delaware and
Val Verde Basins from Lea
County, New Mexico to Edwards County, Texas" (a vertical section map of an
oil producing area).
14lnformation on the structure and density of
mollusk and
arthropod shells or exoskeletons can be obtained from standard works
in paleontology,
such as:
Easton, W. H., 1960, Invertebrate Paleontology: Harper and Row, Inc.,
701 p.
Shrock, B. R., and Twenhofel, W. H., 1953, Principles of Invertebrate
Paleontology: McGraw-Hill
Book Go., 816 p.
Information on the specific location of various species in local stratigraphic
columns can be obtained from well drilling records, and from works on specific
geologic formations and periods in a restricted geographic area. For
example many
such sources are listed on pages 154162 of Bibliography of Permian
Basin Geology,
West Texas and Southeastern New Mexico, West Texas Geological
Society, 1967.
Horowitz, A. S., and Potter, P. E., 1971, Introductory
Petrography of Fossils: Springer-Verlag Company, New
York, 302 p.
15Rrown, C. W., 1961, "Cenozoic stratigraphy and structural
geology, northeast
Yellowstone National Park, Wyoming and Montana": Geol. Soc. America
Bull.,
vol. 72, p. 1173-1194.
Dorf, E., 1960, "Tertiary fossil forests of Yellowstone
National Park, Wyoming": in Billings Geological Society
Guidebook (Eleventh
Annual Field Conference), p. 253-260.
____ 1964, "The petrified forests of Yellowstone
Park": Scientific American, vol. 210, no. 4 (April 1964), p. 106-114.
l6Ewing, J,, and Ewing, M., 1967, "Sediment distribution on the mid-ocean
ridges with respect to spreading of the sea floor": Science, vol. 156, p.
1590-1592.
Ewing, M. Ewing, J. I., and Talwani, M., 1964, "Sediment
distribution in the oceans-the Mid-Atlantic Ridge": Geol. Soc.
Amer. Bull.,
vol. 75, p. 17-36.
Gartner, S., Jr., 1970, "Sea-floor spreading, carbonate dissolution level, and the nature of Horizon A";
Science, vol.
169, p. 1077, 1079.
Pitman, W. C., III, and Talwani, M., 1972, "Sea-floor
spreading in the North Atlantic": Geol. Soc. Amer. Bull,, Vol.
83, p. 619-646,
Vine, F. J, 1966, "Spreading of the ocean floor-new
evidence": Science vol. 154, p. 1405-1415.
17Burek, P. J., 1970, "Magnetic reversals-their applications
to stratigraphic problems": Am. Assoc. Petrol. Geologists Bull. 54,
p. 1120-1139.
Cox, A., Dalrymple, C. B., and Doell, R. R., 1967, "Reversals of
the earth's
magnetic field": Scientific American, vol. 216, no. 2 (February 1967), p.
44-54. Dunn, J. B., Fuller, M. Ito, H., and Schmidt, V, A., 1971,
"Palenmagnetic
study of a reversal of the earth's magnetic field": "Science,"
vol. 172, p. 840-845.
Hays, J. D.. and Opdyke, N. D., 1967, "Antarctic Radio-laria, magnetic reversals, and climatic change":
Science, vol.
158, p. 1001-1011.
Foster, J, H., and Opdyke, N. D., 1970, "Upper Miocene to Recent magnetic
stratigraphy in deepsea sediments': Jour. Geophys. Research, vol. 75,
p. 4465-4473.
Strangway, D. W., 1970, History of the Earth's Magnetic Field, McGraw-Hill Book
Ca., 168 p.
18Dalrymple, C. B,, and Lanphere, M. A., 1969, Potassium-Argon Dating:
W. H. Freeman
Co., 240 p.
____and Moore, J. C. 1968, "Argon 40
excess in submarine pillow basalts from Kilauea volcano,
Hawaii": Science, vol. 161, p. 1132-1135.