A GRAVITY AND AEROMAGNETIC SURVEY OF THEthe Santa Isabel quadrangle, 1:20,000 " " . 13. Complete...
Transcript of A GRAVITY AND AEROMAGNETIC SURVEY OF THEthe Santa Isabel quadrangle, 1:20,000 " " . 13. Complete...
12h
UNITED STATES DEPARTMENT OF THE INTERIOR
GEOLOGICAL SURVEY
A GRAVITY AND AEROMAGNETIC SURVEY OF THE
MID-TERTIARY SEDIMENTARY BASIN
ON THE SOUTH COAST OF PUERTO RICO
By
Andrew Griscom and William L. Rambo
Prepared in cooperation with the
Commonwealth of Puerto Rico
Open-file report
1970
This report is preliminary and has not been edited or reviewed for conformity with Geological Survey standards
Contents
Introduction ................. 1
Acknowledgments .........;...... 1
Previous geophysical work .............. 2
Instruments ................... 4f
Survey procedure and control. ........... 5
Gravity data reduction. .............. 8
Data presentation ............... 10
General geology ................ H
Gravity map ................. 16
Gravity interpretation. ............. 18
Discussion of the gravity map and profiles ....... 24
Discussion of other geophysical data . . . . . . ". . . 35
Conclusions and recommendations. .......... 43
References. ................. 44
Illustrations
Figure 1. Index map of the project area in pocke
2. Complete Bouguer gravity anomaly map of
the Sabana Grande quadrangle, 1:20,000 " "
3. Complete Bouguer gravity anomaly map of
the Yauco quadrangle, 1:20,000 . " *
4. Complete Bouguer gravity anomaly map of
the Penuelas quadrangle, 1:20,000 " "
5. Complete Bouguer gravity anomaly map of
the Ponce quadrangle, 1:20,000 " "
6. Complete Bougter gravity anomaly map of
the Rio Descalabrado quadrangle, 1:20,000 " "
7. Complete Bouguer gravity anomaly map of
the Coamo quadrangle, 1:20,000 " "
8. Complete Bouguer gravity anomaly map of
Guanica quadrangle, 1:20,000 " "
9. Complete Bouguer gravity anomaly map of
Punta Verraco quadrangle, 1:20,000 " "
10. Complete Bouguer gravity anomaly map of
the Punta Cuchara quadrangle, 1:20,000 " "
11. Complete Bouguer gravity anomaly map of the
Playa de Ponce quadrangle, 1:20,000 ." "
12. Complete Bouguer gravity anomaly map of
the Santa Isabel quadrangle, 1:20,000 " "
. 13. Complete Bouguer gravity anomaly map of
the Salinas quadrangle, 1:20,000 " "
Figure 14. Complete Bouguer gravity Anomaly map of
the Ponce area, Puerto Rico, 1:60,000 in pocket
15. Gravity profiles A-A 1 and B-B 1 " "
16. Gravity profiles C-C 1 and D-D 1 " "
17. Gravity profiles E-E 1 and F-F 1 " "
18. Gravity profiles G-G 1 and H~H' ." "
19. Gravity profiles J-J 1 and K-K 1 " "
20. Gravity profiles L-L 1 and M-M 1 . ' " "
21 Gravity profile N-N 1 " "
22. Computed cross-section I-I 1 " "
23. Computed cross-section II-II 1 " "
24. Computed cross-section III-III 1 " "
25. Contoured modified Bouguer anomalies and
surface geologic formations in Puerto . -._-":"
Rico (Shurbet and Ewing, 1956) " "
26. ^Geologic interpretation of gravity map of
the Ponce area, Puerto Rico, 1:60,000 " "
27. Seismograph structural contour map of the
Ponce area of the south coast of Puerto
Rico (Denning, 1948) 1:30,000 " ."
28. Seismograph structural contour map of the
south coastal area of Puerto Rico (Donnally,
1958), 1:30,000 " "
29. Aeromagnetic map of the Ponce area, Puerto
Rico, 1:120,000 " " "
Figure'30. Aeromagnetic profiL les of the south coast of Puerto . .
Rico, 1:50,000
31. Location map for aeromagnetic profiles of the southti »
coast of Puerto Rico, 1:60,000.
Tables
Table 1. Generalized log of test well No. 1CPR 14a
2. Generalized logs .of test well No. 2CPR 14b
3. Generalized log of test well No. 3CPR - 14c
4. Principal facts for the gravity data from
the south coast of Puerto Jlico in separatefolder
Introduction
During the period November 18, 1963 to December 3, 1963 the U.S.
Geological Survey in cooperation with the Commonwealth of Puerto Rico
performed a gravity survey of the Tertiary sedimentary basin which is
located along the south coast of Puerto Rico in the vicinity of Ponce.
The project was initiated at the request of Mr. Carlos Vincenty', Director,
Department of Industrial Research, Economic Development Administration
of the Commonwealth of Puerto Rico. The purpose of the survey was to\
obtain information on the configuration arid structure of the basin and,
if possible, to locate areas which might be favorable for the accumulation
of oil or gas. The accompanying index map (fig. 1) shows the survey area
together with the outline of the border of the basin.
Acknowledgments
We wish to thank Mr. Carlos Vincenty, Director, Industrial Research,
Economic Development Administration, for his advice and assistance con
cerning the field operations of the project. Several geologists of the
U.S. Geological Survey, in particular Mr. Watson H. Monroe and Mr. Peter
H. Mattson, gave generously of their time and knowledge of the area. Other
members of the geophysical field party were Messrs. Gordon E. Andreasen,'
Jack L. Meuschke, James A. Pitkin, and Peter Popenoe. Mr. Randolph W.
Bromery, accompanied by the senior author, during November and December
of 1962, established the gravity bases at San Juan'and Ponce, and tied
them to Washington, B.C. The two gravity stations on Isla Caja de Muertos
were established at this time.
Previous geophysical work
Previous gravity data in the project area are provided by the U.S.
Coast and Geodetic Survey 1929 pendulum base at Ponce and the gravity
reconnaissance survey of Shurbet and Ewing (1956). The data of Shurbet
and Ewing (1956) include 48 stations within the area of this project and
an additional 25 stations from outside the project area which assisted
the contouring of the present survey.
From October 1947 until June 1948 United Geophysical Company, Inc.,
Pasadena, California, conducted a reflection seismograph survey of the
south coast Tertiary sedimentary basin, not only on land but also offshore.
The survey was contracted by the Puerto Rico Industrial Development Company
and the results are contained in a report by W. H. Denning 1948) of United
Geophysical Company. In 1958 the Maritime Oil Company of Houston, Texas,
engaged C. J. Donnally of the Donnally Geophysical Company to review the
records of the reflection seismograph survey. The reinterpretation is
described in a report by Donnally (1958) and an additional geologic report
was written at this time by R. E. Ming (1958), geologist for the Maritime
Oil Company.
All of the above-mentioned reports are available for public inspection
in the office of the Department of Industrial Research of the Economic
Development Administration.
An aeromagnetic survey of the Ponce area was flown in 1957 by Canadian
Aero Service, Ltd., Ottawa, Canada, for A. D. Fraser, Rio Piedras, Puerto
Rico. The mean terrain clearance was 500 feet and the flight spacing
varied from 1 to % mile. The map area is essentially that of the Ponce
quadrangle but extends an additional 5 km to the west and to the north
of the quadrangle as shown in figure 29.
During 1960 under an arrangement with the Maritime Oil Company
three test wells were drilled by the Kewanee Interamerican Oil Company
in the south coast Tertiary sedimentary basin. Each well penetrated
volcanic rocks beneath the unconformity which is found at the base of
the Oligo-Miocene sedimentary rocks. Although no oil or gas was en
countered, the wells provide valuable control for the geophysical data.
In November and December 1961, the U.S. Geological Survey obtained
east-west aeromagnetic profiles over the land portion of the project area
at a one-mile flight spacing and a flight elevation of 500 feet above the
ground. Those data are presented later in this report. In July 1962,
the U.S. Naval pceanographic Office obtained a few widely spaced aero-
magnetic profiles over the offshore portion of the project area at a
flight elevation of 1,000 feet. These profiles are part of a larger
survey flown by the Project MAGNET aircraft to provide data requested by
the National Academy of Sciences in connection with project MOHOLE.
Instruments
-Two gravimeters were used in this survey, each meter being used to
measure approximately half of the 665 gravity stations. A LaCoste and
Romberg Model G gravimeter with a dial constant of 1.0445 mgal per dial
division provided the necessary control for the base stations and a
Worden gravity.meter with a dial constant of 0.53875 mgal per dial
division made it possible to survey rapidly the. closely-spaced stations
along road profiles. After tidal corrections, the drift of the Worden i meter was very linear at the rate of about 0.5 mgal per day and observed
gravity readings were accurate to ±0.1 mgal. The observed gravity
readings of the LaCoste and Romberg meter after tidal corrections were
accurate to within ±0.05 mgal except on one day when a tare or step in
the drift curve introduced an uncertainty of ±0.1 mgal in about 25
stations.
Survey Procedure and Control
Base stations were occupied in the morning and in the evening as
a check on instrument drift. Early in the survey intermediate bases
were also occupied during the day but it was soon demonstrated that when
tidal corrections were applied to the data both meters displayed a very
linear drift so that the practice was not rigorously followed, the
reoccupation of about 25 stations served as a check on the quality of
the data and confirm the conclusions of the previous section concerning
accuracy. It appears likely that the rather small daily temperature
changes to vfaich the meters were exposed contributed to the excellent
performance. Approximately 665 gravity stations were occupied in an
area of 1600 1cm2 .
In order to maintain accurate known elevations, stations were located
at bench marks, sea level, spot elevations such as road junctions, -or
along road profiles where elevations were surveyed with a transit. The
spot elevations and the surveyed elevations are the least accurate and
may be in error by as much as ±0.6 m which represents an uncertainty of
±0.1 mgal in the Bouguer anomaly.
The gravity stations were located to within ±0.01' of latitude on
the U.S.G.S. 1:20,000 quadrangle maps. This latitude uncertainty introduces
an insignificant error of approximately'±0.01 mgal in the Bouguer anomalies.
All of the gravity stations are tied to the project base at the
Ponce Intercontinental Hotel parking lot in the north corner which is
most distant from the hotel or to the U.S.Ceand G.S. Ponce pendulum base
described below. These bases were tied to the U.S.C. and G.S. pendulum
base in the House of Representatives at San Juan and the San Juan base
was in turn tied to the outside gravity bench at the Department of
Commerce Building in Washington, D.C. The observed gravity values for
the more important bases are tabulated below in gal; the additional
figure on the Puerto Rico bases requires the assumption of a value of
980.11820 for the Commerce Building base:
Ponce Intercontinental Hotel 978.60934
U.S.C.&G.S. Ponce pendulum base 978.62784
House of Representatives, San Juan 978.67552
Commerce Bldg., Washington, D.C., 980.1182
outside gravity bench (Behrendt
and Woollard, 1961)
It was not possible to reoccupy exactly the U.S.C. and G.S. Ponce
pendulum base. The location finally used was on the curb at the southeast
corner of the junction between Martin Corchado and Capitan Correa (formerly
Munoz Rivera) Streets.
In order to make use of certain gravity stations from the survey of
Shurbet and Ewing (1956) the observed gravity values of 31 duplicated
stations in the Ponce area were compared. The values measured by the
Lamont group are an average of 3.6 ragal higher than the values in this
report. The Lamont group's value for the Ponce pendulum base is also
higher by 3.6 mgal. As a further check, the complete Bouguer anomaly
values from each duplicated station were compared. In this case the
Lament group's values are an average of only 1.6 mgal higher than the
station values in this report. There thus appears to be a consistent
difference of 2.0 mgal between the terrain correction values used by
the Lament group and those determined for this report. The difference
is unexpected because the method of calculation and the assigned density
are believed to be the same in each case. At any rate all the complete
Bouguer anomalies (modified Bouguer anomalies of Shurbet and Ewing, 1956)
borrowed from the Lament group survey were reduced arbitrarily by 2 mgal
(1.6 mgal rounded) in order that they would better approximate the datum
level of this report.
Gravity Data Reduction
The simple Bouguer anomalies were calculated by means of a computer
program which (after removal of drift and tide correction) applied to the
meter reading the meter scale factor, the latitude correction taken from
the International Gravity Formula of 1930, and the elevation correction.
Densities of 2.67 and 2.27 were used to compute the Bouguer correction.
Because in general the stations at higher elevations are on rocks approxi
mating a density of 2.67 (Bromery and Griscom, 1964), this density was
adopted for the contour maps and profiles. The lower density value is
believed to approximate the density of the Tertiary rocks. The maximum
difference between the two Bouguer anomalies over areas of low density
Tertiary sediments is 3.15 mgal at station 1034 because of its unusually
large elevation (118 m.) 0 The difference between the anomalies for
stations on the Tertiary sediments is usually less than 0.5 mgal.
Terrain corrections were applied to all stations by means of the
Bullard modification of the Hayford-Bowie method (Swick, 1942) out to a
distance of 166.7 km (zone 0) It was found possible to prepare contour
maps of the terrain corrections for zones J through L and a combined map
for zones M, N, and 0. In addition up to three separate contour maps
were prepared for the changes in each zone's terrain correction with
station elevation. Thus by a series of double interpolations it was
possible to obtain accurate and mutually consistent values for the
8
gravitational effects of the topography of zones J through 0 and
simultaneously to save a considerable amount of time. The land and
near-shore ocean bottom topography was obtained from U.S. Geological
Survey topographic maps at scale of 1:20,000, 1:120,000, and 1:240,000.
The elevations of oceanic terrain compartments were determined from the
U.S. Coast & Geodetic Survey chart 920 and U.S. Naval Oceanographic
Office charts 0703N and 0704N. A correction for curvature of the earth
was also subtracted from the station values,, The range of the complete
terrain corrections is from 8 to 12 mgals, most of which is caused by
zones from J through 0.
Earth tide corrections, amounting to a maximum of 0.3 mgal, have
also been applied to all gravity stations. These corrections were obtained
from the tabulated values for 1963 published in Geophysical Prospecting,
vol. X, Suppl. No. 1, December 1962.
The major sources of inaccuracies are caused by instrument reading
errors and drift uncertainties in the observed gravity. It is estimated
that the complete Bouguer anomalies are accurate to within about ±0.5 mgal,
assuming that the charts of the ocean bottom are reasonably accurate.
However, the relative accuracy between nearby stations is much better
because of the procedure described above. The' smoothness of the detailed
gravity profiles is evidence that the relative accuracy of the anomalies
is approximately ±0.1 ragal. Hence the features on the gravity map only
reflect subsurface mass distributions.
Data Presentation
The accompanying tabulation of print-out results from the U.S.
Geological Survey computer lists the principal facts for the gravity
stations together with an explanation of each column of the table.
The complete Bouguer anomalies for each station were plotted on stable
transparent base maps at a scale of 1:20,000 and contoured. Copies of
each contoured quadrangle (figures 2 to 13) accompany this report. In
addition, each contoured quadrangle was photo-reduced to a scale of
1:60,000 and mosaiced together to fit another base map (figure 14).
After contouring the 1:20,000 quadrangles, the various detailed
gravity profiles along roads were plotted (figures 15 to 21) and three
profiles across critical portions of the gravity map were selected for
detailed computation and analysis (figures 22 to 24). Discussion of
these profiles is deferred to a subsequent section of this report.
10
General Geology
Structurally Puerto Rico forms a broad anticlinorium, the axis of
which trends roughly east-west. The project area is on the south flank
of this structure. Here an older basement complex of serpentinite and
related rocks is overlain by a sequence of interbedded volcanic and ,
sedimentary rocks ranging in age from late Cretaceous to middle Eocene.
These rocks are moderately to intensely folded and are cut by numerous
normal, transcurrent, and thrust faults (Glover and Mattson, 1960).
Locally intruding these rocks in the project area are plutonic igneous
rocks ranging in composition from diorite to granodiorite. Unconformably
overlying all these rocks are the Oligocene and Miocene rocks of the south
coast Tertiary sedimentary basin, the prime concern of this report. All
rocks older than the Tertiary sedimentary rocks of the south coast
sedimentary basin will be termed basement in this report, although many
of these older rocks are sedimentary, rather than igneous or metamorphic.
The individual rock units are described in greater detail below.
The oldest known rocks in Puerto Rico are those of the Bermeja Complex
of Mattson (1960) which in the project area is almost entirely composed of
serpentine together with minor chert and altered mafic igneous rocks .
This rock unit forms the cores of anticlines in southwestern Puerto Rico
and is unconformably overlain by rocks of Upper Cretaceous (Campanian) age *>
(Pessagno, 1960). The complex has importance here because gravity surveys . /^
in the Mayaguez area of southwestern Puerto Rico (Bromery and Griscom, 1964)
11
have shown that gravity lows ranging in amplitude .up to 10 mgal are
associated with the serpentinite masses in the anticline cores. A belt
of these rocks is found in the northwest corner (Briggs, 1964) of the
project area extending southeast from the mountains north of Sabana
Grande toward Palomas beneath the basin sediments. A second isolated
exposure of the serpentinite (Grossman, 1963) is in the eastern portion
of. the anticlinal area 1 km west of Central San Francisco where pre-Tertiary
rocks are found surrounded by the Oligocene and Miocene sedimentary rocks.
The majority of the basement rocks are interbedded volcanic and sedimentary
rocks containing a few small masses of intrusive rocks. In the north
eastern portion of the project area these Cretaceous and Eocene rocks
are described as follows by Glover (written communication, 1965): "about
90 percent are marine pyroclastic and reworked marine pyroclastic rocks,'
and 10 percent are subaqueous lavas and limestones." The rocks at the
extreme western border of the project area are tuffaceous mudstone and
sandstone, limestone, pyroclastic rocks, and both andesitic and basaltic
lava flows (Mattson, 1960), the units having an aggregate thickness of
at least 4000 meters.
The geology of the sediments and sedimentary rocks of the south
coastal plain has been described by Zapp, Bergquist, and Thomas, 1948.
More recent information for portions of the area is found in Grossman
(1962, 1963), Slodowski (1956), Pessagno (1960a), and unpublished maps
of the Rio Descalabrado and Santa Isabel quadrangles by Glover and Mattson
and of the playa de Ponce quadrangle by Glover, Pease and Arnow. Recent
unpublished geologic mapping by W. H. Monroe (written communications,
12
1969 and 1970) indicates that substantial revision is needed in the
geology of the middle Tertiary rocks as described by Zapp, Bergquist
and Thomas (1948). "
The older of the two named rock units, the Juana Diaz Formation,
ranges in age from lower Oligocene (Seiglie and Bermudez, 1969; Ruth Todd,
unpublished data) through middle Oligocene (Grossman, 1962) and perhaps
into the Miocene, depending on the definition of the formation (Monroe,
written communication, 1970). The lithology is primarily clastic;
sandstone, conglomerate, mudstone, and shale. Thicknesses range from
only a few meters to a local maximum of at least 1300 ra. at or north of
Palomas near Youco (Grossman, 1962) and locally the formation is missing.
Initial dip of the conglomerates may cause overestimates of thickness
(Glover, written communication, 1965). The log of test well No. 3CPR
(table 3) indicates a thickness of about 344 m. of Juana Diaz Formation.
The younger of the Tertiary units is the Ponce Limestone, buff-
colored reef limestone and chalk, ranging in age from upper Oligocene
to Miocene. The lower portion of the unit may intertongue with part of
the Juana Diaz Formation (Monroe, written communication, 1970). Because
of faulting, thickness estimates from geologic mapping are uncertain but
test wells No. 2CPR (table 2) and No. 3CPR (table 3) indicate that the
thickness can locally exceed 260 ra.
A considerable thickness of alluvial deposits conceals the Tertiary
rocks and their contacts throughout much of the coastal plain east of
Ponce where the topographic expression of the Tertiary rocks is relatively
low compared to the area west of Ponce. Well data indicate that the
thickness of the alluvium locally exceeds 150 m and may in fact be
considerably thicker.
13
Subsurface stratigraphic information- for the coastal plain sediments
and sedimentary rocks is provided by the logs of the three test wells
(tables 1 to 3) drilled by the Kewanee Interamerican Oil Company,, The
lithologic logs were made by Thomas N. Ambrose, geologist at the drilling
sites, and subsequently a paleontological study of the well samples was
made by W. Anthony Gordon of Oberlin College. The two sets of data are
not always in agreement and some interpretation is necessary.
The structure of the Oligocene and Miocene rocks of the south coastal
plain is indicated in figure 26 which is based primarily on unpublished -
maps by Glover and Mattson east of lat 66°30'W and on unpublished mapping
by W. H. Monroe (written communications, 1969 and 1970) west of lat
66°30'W, but also on local mapping by Grossman (1962, 1963). The sediments
in general form a south-dipping homocline with dips of 10-30° at the north
side of the belt, diminishing to dips of 4-6° at the coast west of
Guayanilla. Recent geologic mapping by Monroe indicates that west of
Ponce block faulting is very abundant and that the north contact with
the basement rocks is generally a fault. Closure on the syncline northwest
of Juana Diaz is about 225 m (Zapp, and others, 1948). The fault trending
east-west between Guanica and Guayanilla Bay has a dip slip which "is at
least several hundred feet and could be as much as a few thousand feet"
(Grossman, 1963).
14
Table 1
Generalized log of test well No. 1CFR
The below data are by T. N. Ambrose. No detailed paleontological
data are presently available.
Thickness Geologic unit ' Depth (feet) (feet) (meters)
Alluvium (certain fossils 0-2995 2995 913
suggest most of this may
be Tertiary)
Oligocene and Miocene 2995-4270 1275 389
sedimentary rocks
Lower Tertiary or Upper 4270-7480 3210 979
Cretaceous volcanic rocks
14a
Table 2 '
Generalized logs of test well No. 2CPR
Geologic log (T. N. Ambrose)
Th ickness Geologic unit Depth (feet) . (feet) (meters)
Alluvium 0-2875 2875 877
Ponce Limestone 2875-3760 885 270
Shale (Cretaceous ?) 3760-4060 300 91
Lower Tertiary or Upper 4060-4919 859 262
Cretaceous volcanic rocks
Paleontologic interpretation (W. A. Gordon)
Quaternary 0-500+ >500 >152
Ponce Limestone above 590 to above 740 ~150 ~. 46
(upper member)
Ponce Limestone above 740 to above 2890 ~2150 ~656
(lower member)r
Juana Diaz Formation above 2890 to above 3790 ~900 ~274
(shale)
Pre-Oligocene rocks above 3790 to 4919 ~1129 ~344
14b
Table 3
Generalized log of test well No. 3CPR
This log was interpreted by T. N. Ambrose using paleontological
data provided by W. A. Gordon
ThicknessGeologic unit
Beach sand
Gravel and sand (Quaternary alluvium)
Silty limestone (Probably late Tertiary)
Reef(?) limestone (calcarenite)
Ponce Limestone-upper member
Ponce Limestone-lower member
Juana Diaz Formation-shales, (the paleontolog ic contact between the Ponce Limestone andJuana Diaz Formation is in the range 2000-2200 feet)
IINnDNFDRMTTY .._---_ __--
Depth (feet)
0-80
80-110
110-550
550-860
860-1370
1370-1720
1720-2848
(feet)
80
30
440
310
510
350
1128
(meters)
24
9
134
94
155
107
344
Lower Tertiary or Upper Cretaceous volcanic rocks
2848-4141 1293 394
14c
The geology of Isla Caja de Muertos provides valuable information
on the structure of the southernmost portion of the coastal plain. The
Provisional Geologic Map of Puerto Rico shows the geology of the island
as a central area of basement rocks in fault contact to the north and
sedimentary contact to the south with two masses of younger sedimentary
rocks "probably equivalent to the Ponce Limestone" (Briggs, 1964). The
basement rocks (Glover, written communication, 1965) are "tuffs, tuffaceous
plankton-bearing mudstone, and minor intercalations of intraformational
conglomerate" and are believed to correlate with basement rocks in the
Rio Descalabrado quadrangle. The younger sedimentary rock from the south
end of the island is described as follows (U.S. Geological Survey, 1964):
"Conglomerate on Isla.Caja de Muertos... collected by P. H. Matson contains
Eocene larger Foraminifera in pebbles and Oligocene large Foraminifera in
the matrix, according to K. N. Sachs, Jr. The conglomerate is probably
correlative with some of the Oligocene strata in the coastal plain of
southern Puerto Rico. It dips about 35°SE and is overlain unconformably
by subhorizontal limestone also believed to be equivalent to a part of
the Oligocene and Miocene coastal-plain sequence. This relation indicates
that deformation occurred in this area in Oligocene or possibly Miocene
time."
15
Gravity map
The complete Bouguer anomaly map of the project area is shown in
Figure 14, This map is superimposed on a base which is the U.S.
Geological Survey 1:120,000 map of Puerto Rico enlarged to a scale
of 1:60,000. The complete Bouguer gravity anomaly values for the
individual stations are shown on the 1:20,000 maps but are omitted
from the 1:60,000 map, although the station locations are indicated.
The Bouguer anomaly values range from a low of 82,8 mgals on Cayos
Frios at the center of the project area in the Playa de Ponce quadrangle
to a high of 137 mgals (Lamont Group station) in the Coamo quadrangle at
the northeast corner of the project area. In detail the gravity map is
complex but in general the gravity field slopes downward from north to
south across the map and then rises again a few milligals on Isla Caja
de Muertos at the extreme south edge of the project area. This regional
slope southward is caused by a combination of two effects: the increase
in thickness of .the low density Oligo-Miocene sediments to the south; and
a regional gradient resulting from a broad gravity high over the central
portion of Puerto Rico, as shown in figure 25, reproduced from Shurbet
and Ewing (1956). This gravity map of Puerto Rico (figure 25) also
shows the south coast gravity low caused by the low density Oligo-Miocene
sediments.
16
The 1:60,000 gravity map of the Ponce area is (fig. 14) contoured
at a 1 mgal contour interval to take advantage of the.abundant gravity
data along the shore and the detailed north-south traverses. Nevertheless
it must be recognized that in certain portions of the area the station
density is.insufficient to define accurately the location of the.1 mgal
contours. When using this gravity map for detailed local interpretations,
the available local gravity control for the contours must be considered
carefully.
17
Gravity Interpretation
There are three general classes of rock density variations which
may cause the gravity anomalies of Figure 14. The first of these
classes is variation in density of the basement rocks. Examination
of the gravity field along the northern third of Figure 14 discloses
several local gravity features associated with basement rocks. Examples
of such features are: the gravity high near Lago Coamo in the southeast
corner of the Rio Descalabrado quadrangle, the gravity high at Lago
Numero Dos in the center of the Ponce quadrangle, and the gravity high
at Penuelas in the Penuelas quadrangle. Another such feature is the
gravity low 2 km west of Yauco in the northwest corner of figure 14
associated with the northwest-trending anticlinal mass of serpentinite
previously mentioned. This gravity low extends southeast into the
area of Oligo-Miocene sediments, and as described in the subsequent
discussion on calculated profile I-I f (Figure 22), an attempt has been
made to subtract this basement anomaly in order to isolate the gravity
effect of the Oligo-Miocene sediments. The gravity high at Lago Coamo
has an appreciable effect upon the gravity contours near the north edge
of the Tertiary sedimentary basin in this area but this is the only
other clearly identifiable gravity anomaly associated with basement rocks.
In the subsequent discussion of the gravity anomalies over the Oligo-
Miocene sediments, it has been assumed that the anomalies are not caused
by density variations within the basement rocks. If this assumption is
incorrect, large errors may exist in the interpretation.
18
The second class of rock density variation| is the contrast
between the density of the sediments and sedimentary rocks of the
coastal plain and the density of the basement rocks. This density
contrast is relatively large and, in the belief of the senior author,
is the major cause of the variation in gravity anomalies over the
coastal plain.
The third class of possible rock density variation^ occurs within
the coastal plain sediments and sedimentary rocks. Such density
variations may be both vertical and lateral. The major evidence for
such variations is provided by the three test wells (see tables 1, 2,
and 3) and to some extent the seismic data, (fig. 27 and 28) if the
reflecting horizons indicate a density change. Test well 1CPR indicates
2995 feet of alluvium and 1275 feet of Middle Tertiary sedimentary rocks,
Test well 2CPR indicates either 500 feet or 2875 feet of alluvium and,
respectively, 3200 feet or 885 feet of Middle Tertiary sedimentary
rocks, depending on which interpretation is favored. Test well 3CPR
indicates 110 feet of unconsolidated sediments, 750 feet of limestone
of uncertain age, and 1988 feet of Middle Tertiary sedimentary rocks.
19
The data from the wells show that a substantial thickness of alluvial
deposits may overlie the Middle Tertiary sedimentary rocks in some
areas, especially to the east of long 66°30'W. In addition the data
from test well 3CPR can be interpreted to indicate that reef limestones
may have been deposited contemporaneously with the alluvial material
but to the south sof^i* at or near the former shoreline. If this is
true, there may be lateral 1 density variations within the sediments and
sedimentary rocks overlying the Middle Tertiary rocks, the higher
density material being reef or other marine limestones located to the
south of the alluvial sediments. The subsequent discussions will
explain why the writers believe that the effects of possible vertical
and lateral density changes on the local gravity field are quantitatively
less important than the effect of the density contrast between basement
rock and the overlying basin deposits.
Information on basement rock densities from southwest Puerto Rico
is found in Bromery and Griscora (1964), where an average density of
2.70 g/cm3 was determined from 29 samples of volcanic and sedimentary
rocks. Densities ranged in value from 1.70 to 2.98 and 19 of these
values were within the range 2.60 to 2.80. An average density of 2.55
g/cm3 was also determined from approximately 160 samples of serpentinite.
Long detailed gravity profiles in north-central and southwestern Puerto
Rico, having a station spacing of about 600 feet across areas of basement
rocks other than granitic plutons, are very smooth and show anomalies of
only a few mgal. Such results suggest that the average bulk densities
of these older volcanic and sedimentary rock units are relatively
constant, or vary slowly over large distances.
20
The density of the Middle Tertiary calcareous rocks is uncertain
because of several factors: surface samples are unreliable due to
weathering and "case-hardening" by filling of pore-spaces with calcite;
fresh quarried samples are often sufficiently unconsolidated that they
can be excavated by power shovel; the rocks at greater depth are
subject to incipient dolomitization and recrystallization which may
increase their density relative to near-surface samples. Six samples
from a rather typical Middle Tertiary calcarenite on the north coast
(Briggs, 1961) at a depth of approximately 3700 feet ranged in density
from 2.20-2.59 and had an average density of 2.40. The material logged
as alluvium in wells 1CPR and 2CPR is probably somewhat lower in density
than the Middle Tertiary limestones because of increased porcrsity but
the average density is very uncertain. Measurements of densities of
well cuttings from the three south coast test wells have not yet been
made but will not provide very useful density data with which to interpret
the gravity map. Cuttings from relatively porous sedimentary rocks give
densities substantially higher than in situ average densities. Cuttings
from alluvial material, especially gravels, give densities which have
little meaning relative to average alluvium density. Well-logging by
various geophysical techniques will ultimately provide the best density
information.
21
In this study, because of the uncertainty concerning rock
densities, it seemed best to calculate the average density contrast
between the coastal plain rocks and the basement by using the known
depth to basement together with the known gravity in the vicinity of
the test wells. The calculated density contrast is 0.4 g/cm 3 (0.425
for profile III, figure 24) which means that the average density of
the coastal plain rocks is approximately 2.30 g/cm3 , assuming an average
density of 2.70 g/cm3 for the basement rocks. This calculated density
contrast is subject to some uncertainty because a regional gradient
must first be deduced and subtracted from the gravity data before pro
ceeding with the calculations. The gravity data indicate further that
the regional gradient is curved in the eastern portion of the project
area, but is probably nearly linear in the western portion. The deduced
regional gradients shown on calculated profiles I-I ! , II-Il', and Ill-Ill 1
(Figures 22, 23, and 24) are progressively more uncertain to the south
as the distance increases from the exposed basement rocks but the exposed
basement on Isla Caja. de Muertos provides valuable control.
The average density of 2.3 g/cm3 calculated for the Tertiary and
Quaternary sediments and sedimentary rocks of the coastal plain is
reasonable. The near-surface semi-consolidated alluvial deposits when
water-saturated may have an average density of less than 2.0 g/cm3 but
some of the more massive limestones in the Ponce Limestone probably
have densities in excess of 2.5 g/cm3 and certain shales of the Juana
Diaz Formation when water-saturated may well have densities greater
than 2.4 g/cm3 . It seems possible that the Middle Tertiary sedimentary
22
rocks may have an average density as high as 2.40 g/cm 3 , in which
case the overlying younger material could have an average density as
low as 2.25 g/cm 3 in the vicinity of profile Ill-Ill f (fig. 24).
However, the calculation for probile II-II* (fig. 23) passes through
test well 3CPR which penetrated a relatively small thickness of
unconsolidated material compared with the relatively large thickness
of limestone and shale. Yet for this profile the calculated density
contrast is also 0.4 g/cm3 so that the density of the Tertiary rocks
is here probably 2.30 g/cm3 ., The evidence thus favors the interpreta
tion already mentioned, namely that density variations within the
Quaternary and Tertiary section are relatively small compared with
the density contrast between these rocks and the basement.
From the preceding discussion it can be seen that in this report a
gravity high will be interpreted as a local area where the coastal plain
rocks are relatively thinner than in adjacent areas and conversely that
a gravity low represents a local area where the coastal plain rocks are
thicker than in adjacent areas. A steep gravity gradient is interpreted
as the location of a zone of rapid thickening of the sedimentary rocks,rf
caused either by deposition against a steep slope or by folding and/or
faulting. If the gravity gradient is particularly steep and also linear,
it is deduced to be the expression of a fault which offsets the basement-
sediment interface. As shown in Figures 22, 23, and 24, it may be
possible to calculate the approximate dip of the fault surfaces from the
gravity gradients.
23
Discussion of the Gravity Map and Profiles
..In order to obtain a better understanding of the gravity map,
three gravity profiles were constructed across suitable portions of
the map, and the two-dimensional geologic configuration of'the base
ment surface necessary to produce the observed gravity anomalies was
calculated using the iterative computer program developed by M. H. P.
Bott. The profiles were constructed approximately normal to the
gravity contours and located to pass close to the test wells and
inliers of basement rocks in order to provide adequate control for the
calculation.
The calculated configuration of the basement surface is a con
siderable oversimplification of the actual configuration for several
reasons. Local minor relief of the basement surface cannot be detected
by the method used. Some of the steeply dipping basement-sediment
interfaces may in detail be a series of step faults or a combination
of faulting and folding. The assumed density distribution is considerably
oversimplified and the deduced regional gradients are subject to
increasing uncertainty toward the southern end of the profiles. Lastly,
the assumption of two-dimensionality is not strictly valid because the
anomaly patterns are not entirely linear normal to the profiles. As
previously mentioned, it is because of these various uncertainties
that no attempts have been made at more refined calculations using three-
24
dimensional assumptions. Nevertheless the writers believe that the
three calculated profiles (Figures 22, 23, and 24) represent a
reasonable, although generalized, approximation of the basement con
figuration.
Calculated profile I-I 1 (Figure 22) is located at the west end of
the gravity map (Figure 14). This profile passes very close to an
inlier of basement rocks which here are serpentinite (Grossman, 1963).
The inlier confirms the deduced linear extension to the southeast of
the bordering serpentinite mass under the sediments of the coastal
plain. This deduction is made on the geologic evidence. The gravity
low associated with this serpentinite is thus superimposed upon the
gravity field of the coastal plain sediments. An asymmetric gravity
minimum of 7.5 mgal is assumed to represent the gravity effect of the
serpentinite mass, by analogy with the observed gravity effect on
parallel profiles across the mass northwest of the coastal plain sediments,
and the minimum has been subtracted from the initial residual gravity
profile to give a resulting curve, the residual gravity without the
effect of the serpentinite mass. This final profile is assumed to
represent only the gravity effect of the coastal plain sediments.
25
The calculated basement configuration indicates a maximum thickness
of about 1250 feet for the sediments of the coastal plain north of
the inlier. In this same general area geologic mapping (Grossman,
1962) indicates that the total thickness of sediments may be about
4000 feet. Possible sources of error in the gravity calculation are
overestimation of the gravity anomaly caused by the serpentinite and
an assumed density contrast (0.4 g/cc 3 ) which may be too large in this
area because the sediments are primarily the Juana Diaz Formation.
Nevertheless it is difficult here to reconcile the gravity data with
the geologic estimate of sediment thickness. Two inflection points on
the profile, respectively 0.5 and 2.0 km north of the inlier, may
represent normal faults downdropped on the north side. The first fault
probably corresponds with the fault mapped by Grossman (1963) bounding
the north side of the inlier. Judging by the gravity data, the throw
on these faults can hardly exceed a few hundred feet. Another inflection
on the profile is located about 3 km south of the inlier and may represent
a small fold but the gravity control is not sufficiently complete in thisc.^2^
area (Figure 14).
26
Calculated profile II-II 1 (Figure 23) passes near test well 3CPR
in the center of the project area thus providing an opportunity to
calculate the regional gradient north of the well. South of the test
well the regional gradient must level off somewhere in the southern
portion of the project area (Figure 14) because oceanic depths are
found only a few km beyond the south end of the profile and here the ,
Bouguer gravity values are rising towards typical oceanic values of
about 300 mgal. In addition the regional gradient must level off
because basement rocks are exposed on Isla Caja de Muertos. When the
regional gradient is assumed to be horizontal, as shown, the calculated
gravity profile indicates that basement rocks approach the surfa.ce at
the south end.
The gravity calculation of profile II-II 1 indicates that test well
3CPR was drilled on a basement uplift which may be faulted on the south
side, judging by the steepness here of the gravity gradient. Basement
depth south of this fault is probably a maximum for the project area,
reaching depths of at least 6500 feet below sea level. The area of
maximum depth lies south of the shoreline where no gravity data are
available. The data on Isla Caja de Muertos when projected on to profile
II-II 1 suggest that basement depths between the island and the Puerto
Rico south coastline are unlikely to exceed 8000 feet because of the
relatively high gravity values on the island, coupled with the basement
outcrop.
27
North of test well 3CPR a small basement depression 4 km east
of Playa de Ponce is calculated on profile II-II 1 to have a maximum
depth in excess of 5000 feet. This basin is likely to be somewhat
deeper than calculated because it is not truly two-dimensional in plan.
The final calculated profile (Figure 24) is along section Ill-Ill 1
which trends approximately N17E through the delta of Rio Descalabrado
(Figure 14).- The offshore portion of this profile is rather uncertain
because the gravity contours have been inferred from the shore data and
the gravity stations on Cayo Berberia. Nevertheless a northwest-
trending basement ridge is probably present about 3 km offshore. The
southwest margin of this ridge is located at Cayo Berberia where the
usually steep gravity gradient suggests a possible fault with the down-
thrown side on the southwest (Figure 24). This fault may connect with
the similar fault on profile II-II 1 . The maximum offshore depth to
basement is unlikely to exceed 7000 feet on this profile, again using
the data on Isla Caja de Muertos as a guide.
28
Profile Ill-Ill 1 passes between test wells 1CPR and 2CPR and the
location of both wells relative to the associated gravity minimum
suggests the measured basement depths are maximum for this part of the
project area. Accordingly a mean basement depth of 4000 feet was
adopted for the calculated profile although a greater depth is possible,
The gravity minimum indicates the presence of a small elongate basement
depression in this area, again somewhat analogous to the depression on
profile II-II 1 . However, the northeast margin of this basin is marked
by a pronounced steep linear gravity gradient, indicating a steeply
sloping basement-sediment interface which is presumably a fault. The
seismic data (Figures 27 and 28) confirm the existence of this fault.
In addition to the calculated profiles, a series of 13 gravity
profiles (Figures 15 to 21) have been constructed from the gravity data
collected along the detailed north-south road profiles. These profiles
can be used to obtain a better understanding of the gravity map and as
a means to obtaining an appreciation of how smoothly the gravity field
varies in this area. The smoothness of the profiles suggests that near-
surface lateral density variations are in general not present which in
turn may imply that near-surface structure has no major faults or folds,
29
After studying the calculated profiles, it becomes possible to
evaluate better the contoured gravity map (Figure 14) of the project
area. The results of this evaluation, together with the basement
depths from the test wells and calculated profiles, are plotted on
the geologic interpretation map (Figure 26). The steep gravity
gradients, especially in the eastern third of the project area, .are
extremely linear and mark the location of a major fault bounding the
northeast margin of the Tertiary sedimentary basin. The fault zone
appears to be interrupted by a basement feature north of Santa Isabel.
This fault parallels a system of major faults of early Tertiary age
(Glover and Mattson, 1960; Briggs, 1964) cutting exposed basement rocks
along the northeast boundary of the project area and indicates that
portions of the fault system were active subsequent to the development
of the unconformity between the Eocene volcanic rocks and the Oligocene
sediments of the Juana Diaz Formation.
A northeast-trending fault is interpreted to be located near the
shore of Bahia de Guayanilla in the western portion of the project area.
This fault appears to be the eastern extension of the fault mapped by
Grossman (1963) on the north side of the serpentinite inlier and has the
same sense of movement, i.e. down on the north side.
30
The gravity contour map indicates a rather curvilinear pattern of
gravity highs and lows which are shown as interpreted basement ridges
and troughs on .the geologic interpretation map. Trend directions vary
from northwest through east-west to southwest. Although these features
are shown on the map as ridges and troughs, it is possible that they are
associated on one or both sides with faults.
The folds clearly established by geologic mapping are shown on
figure 26 and are the syncline at Juana Diaz, the anticline located
about 1 km south of the town, the anticline southwest of Penuelas, and
the folds west of Central San Francisco. The gravity expression of the
features near Juana Diaz is small, amounting to 1 or 2 i-igal, but can
nevertheless be clearly seen on the gravity map and on profile K-K f
(Figure 19).
Although the above-mentioned major gravity features are linear,
they clearly vary considerably in amplitude along their trends so that
the deepest or shallowest portions of each feature occur in relatively
restricted areas. This conclusion is a result of the pattern of somewhat
isolated and relatively equidimensional gravity highs and lows. From
east to west the following major local gravity highs and lows are
evident: a high 2 km south of Santa Isabel, a low at Playa Cortada, a
high 2 km west of Pastille, a low 5 km east of Playa de Ponce, a broad
high about 7 km west of Ponce, a low 3 km south of Guayanilla, and a high
associated with the basement inliers about 3 km west of Central San
Francisco. The gravity highs associated with the known basement high
31
west of Central San Francisco and with Isla Caja de Muertos can be used
as additional evidence that basement highs are possible and may be the
cause of the gravity highs elsewhere in the project area. By using
the regional gradients deduced from the calculated profiles, it is
possible to estimate the difference between the. gravity anomaly over
these basement highs and the amplitude of the regional gradient anomaly
at the same place. Then from this residual anomaly a basement depth
may be calculated. The residual anomaly for the basement highs south
of Santa Isabel and west of Pastille is estimated to be approximately
-10 mgal (i.e. the top of the high is 10 mgal below the regional gradient),
The calculated basement depth associated with these two gravity features
is approximately 1500-2000 feet, the former feature being perhaps slightly
shallox^er than the latter. More exact calculations seem unx^arranted
because of the uncertainty in the regional gradients.
The broad gravity high about 7 km west of Ponce is a more puzzling
feature. No gravity data are available over the central portion of this
high and it is possible that the inferred contours are not entirely
correct and that the feature may not be connected with the small local
gravity high near the town of Penuelas. The association of the feature,
with Middle Tertiary sedimentary rocks suggests some cause and effect
relationship. The Middle Tertiary sedimentary rocks are well exposed
in this area and appear to form a monoclinal structure dipping
32
gently south. The east-west topographic grain in this area confirms
the geologic data. It can be noted that the gravity contours rather
closely follow around the south margin of this topographically high
area and thus also follow the contact between the Tertiary rocks and
the overlying Quaternary sediments and sedimentary rocks. It may be
that some of this gravity high is caused by a density contrast between
the Oligo-Miocene rocks and the Quaternary sediments and sedimentary
rocks, but the anomaly has so substantial an amplitude that it must
be primarily caused by a basement-Tertiary rock density contrast.
In addition, the narrow gravity trough on the northeast side of the
high is almost certainly not caused by the alluvium. The association
of the anomaly with a regional topographic high suggests that this area
may have been uplifted in post-Miocene time relative to adjacent areas
of Oligo-Miocene rocks, presumably by means of faulting. A possible
location for such a fault (figure 26) on the northeast side of this
gravity high is the steep gravity gradient trending northwest from Los
Pampanos which is situated 3 km southwest of Ponce. Using the geologic
cross-section of Zapp, Bergquist, and Thomas (1948) through this gravity
high, the estimated stratigraphic thickness of the Middle Tertiary
sedimentary rocks is nearly 6,000 feet at the coastline, yet test well
3CPR on strike 13 km to the east apparently penetrated only 1,988 feet
of these rocks and additionally is 15 mgal lower than the corresponding
place at the south end of the cross-section 13 km to the west. There
33
are evidently structural complications here in the Middle Tertiary
sedimentary rocks and such complications evidently involve duplication
by faulting of 'the stratigraphy in the area of the gravity high west of
Ponce. Further evidence bearing on the postulated fault extending
northwest from Los Pampanos is provided by Glover (written communicant ion,
1965) who points out that reconnaissance data suggest a major fault in
the basement strikes southeast into the Los Pampanos feature. If so,
density variations within the basement may explain part or all of the
gravity feature or, alternatively, the fault may have been reactivated
subsequent to deposition of the Middle Tertiary rocks.
The gravity lows at Playa Cortada and 5 km east of Playa de Ponce
have already been described in the .section on the calculated gravity
profiles. The gravity low 3 km south of Guayanilla has an amplitude of
only about -15 mgal relative to the regional gradient and maximum basement
depth here will probably not exceed 3,500 feet, especially if some of
this minimum is caused by an underlying serpentinite mass.
34
Discussion of Other Geophysical Data
- The most valuable geophysical information complementing the south
coast gravity survey is the reflection seismograph survey conducted in
1947 and 1948 by United Geophysical Company, Inc. The results of the
interpretation of this survey are contained in a structure contour map,
plate III of the report by Denning (1948). A rough copy of plate III
is included as Figure 27 in the present report. The results of the
1958 reinterpretetion of the seismic data by C. J. Donnally are summarized
in two rather similar structure contour maps in his 1958 report. A copy
-of .one of these maps is also included in the present report (figure 28).
A subsequent reevaluation of the seismic survey was made in 1962
by D. R. Mabey of the U.S. Geological Survey (Mabey, written commun.., .
1963) c Mr. Mabey's comments are so important, relative to the interpre
tation of the gravity survey, that liberal use has been made of quotations
from his communication . His overall evaluation of the maps is as follows:
"In general the structure indicated on United's contour map of the south
area appears to be a reasonable interpretation, of the seismic data.
However, the contours probably are not on a single horizon. I was unable
to duplicate much of the interpretation shown on Donnally's structure maps."
As pointed out by Mabey, none of the structure contour maps give any
indication of the degree of reliability of the reflection data for different
portions of the maps so that it is not possible to decide upon the relative
35
probability of some of the structures without referring to the original
data. On the Donnally Geophysical Company map (Figure 28) only one
basement high with closure (feature "B" near Santa Isabel) correlates
with a gravity high on Figure 14. There is no gravity evidence to
substantiate the interpreted faults on the land portions of the two
Donnally maps. The true basement depths at the test wells ICPR and
2CPR differ by approximately 15 percent from the basement depths
indicated on Figure 28. The major contribution of the maps and report
of the Donnally Geophysical Company is the recognition of a probable
unconformity within the Oligo-Miocene sediments because of abrupt
steepening of the dips of reflecting horizons below certain depths
on the seismic records. In general the depths indicated on Figure 28
are roughly the same order of magnitude as those deduced from the gravity
data but the structure interpreted from the two kinds of geophysical
data is dissimilar.
The United Geophysical Company map (Figure 27) is contoured on
relatively shallow reflecting horizons which may not everywhere be the
same. If, as appears to be indicated by the seismic data, there is an
unconformity below the contoured horizons but within the coastal plain
sediments, the structures indicated by this map (figure 27) may not all
necessarily correspond with the structure deduced from the gravity data
for the buried basement surface. In particular, the major northeast-
trending anticline shown on Figure 27 north of Santa Isabel is in
36
considerable conflict with the gravity interpretation. However, the
gravity high 2 km west of Pastille, which is believed to represent a
basement high at a depth of only 1,500 feet, correlates exactly with
a closed structural high interpreted to be a depth of 1300 feet on
Figure 27. Elsewhere, the lack of correlation of the seismic inter
pretation with the gravity interpretation may be caused by the afore
mentioned intervening unconformity.
Mabey states that in the vicinity of the three test wells there was
no evidence of reflections from the top of the basement and no usable
reflections within the basement. He further writes that "since all
the usable reflections appear to come from above the basement, it
should be possible to indirectly map tfe basement as being slightly
below the general level of the deepest rcflections " The following
interpretive comments by Habcy are based on this approach. The sedi
mentary section is interpreted to be about 3,000 feet thick 2 km southeast
of Salinas and becomes thinner toward the north and east. Mabey further
concludes "that along line U-ll east of SP-49 (shotpoint 49) the sedi
mentary section is generally less than 3,000 feet with the possibility
of a local thickening immediately east of Salinas. The thickest section
along this line is probably between SP-50 and SP-96 where it is at ;
least 4,000 feet thick. West of SP-97 the section ranges in thickness
between 2,500 and 3,500 feet." It can be noted by reference to the
gravity map and the geologic interpretation map (Figure 14 and 26) that
37
the above depth estina tes are in good agreement with the gravity data.
Line U-20 passes north-south through the site of test well 3CPR (basement
depth 2,845 feet). Mabey notes the deepest reflections occur north of
the well at SP-11 where the sedimentary section may be 3,400 feet thick,
suggesting that the well is located on a basement high. Again, the
gravity data clearly substantiate this interpretation, as shown by-
calculated profile II-II 1 (figure 23).
The southward extension of line U-20 is line W-20. Mabey believes
that along this line "the sedimentary section probably thickens southward
with the maximum thickness at the south end of about 5,000 to 6,000 feet
but perhaps as much as 7,000 feet." Along east-west line W-23 nthe
sediments probably thicken eastward from about 3,000 feet at the west
end of the line to 6,000 to 7,000 feet near SP-28. The 3,500-foot
displacement indicated by United (between SP-32 and SP-33) on their
structure horizon is a reasonable displacement on the surface of the
basement complex. . . « Immediately east of the proposed fault the
sediments are probably not more than 3,000 feet thick but thicken
generally eastward to between 4,000 to 5,000 feet near SP-51."
Line W-5 coincides with calculated gravity profile Ill-Ill 1
(figure 24) and Mabey's interpretation of this reflection data agrees
well with the gravity interpretation -considering that the location of
the offshore gravity contours is inferred from scanty data. "The
sediments appear to thin westward from about 4,000 feet to about 2,500
38
feet near SP-14 and SP-15 northwest of Cayo Berberia. This thinning may
indicate a basement high associated with Cayo Berberia, or it may be the
result of the bend in the line. Southwest of this high the section
thickens to between 4,000 and 5,000 feet near SP-18 and SP-24 and then
thins toward Is la Caja de Muertos."
It is concluded that in general the agreement is good between Mabey's
interpretation of the seismic reflection data and this report's inter
pretation of the gravity data. This agreement tends to produce confi
dence in the conclusions of both interpretations.
The aeromagnetic survey flown in the Ponce area in 1957 by Canadian
Aero Service is included in this report (figure 29) at a reduced scale
for the sake of completeness. The area covered by the survey extends
only 2 to 5 km south of the edge of the coastal plain and provides
relatively little information about the project area. The aeromagnetic
data generally indicate a gently south-dipping sediment-basement interface,
although there is some evidence for the northernmost of the two normal
faults 1 km north of Juana Diaz. At the western border of the magnetic
survey strong northwest-trending magnetic lineaments are generated by
the basement rocks. These trends parallel the interpreted fault extending
northwest from Los Pampanos near Ponce and forming the northeast boundary
of the broad gravity high west of Ponce.
39
The aeromagnetic profiles flown by the U.S. Geological Survey in
1961 are displayed on Figure 30 at a scale of .1:50,000. The numbers on
the profiles are location points and these, together with the flight paths,
are also shown on the accompanying location map (figure 31), at a scale of
1:60,000. The one-mile spacing of the flight lines was dictated,by the
original purpose of the survey, a radioactivity survey for the Atomic
Energy Commission, and as a result the magnetic data, although very useful,
cannot be contoured. No attempt has been made at a complete interpretation
of this data, especially insofar as it concerns the variations in basement
lithology, but certain interpretative comments follow which specifically
relate to the gravit}' survey and the interpreted configuration of the
basement surface. Ultimately the major usefulness of data such as this
will be as a guide to detailed geologic mapping of the basement rocks.
For the purpose of interpretation, it is assumed that the magnetic anoma
lies are caused by masses of igneous rocks, here most likely volcanic,
which extend to the upper surface of the basement. The method of interpre
tation used in this section is qualitative only and is based on the prin
ciple that, other factors being equal, more deeply buried magnetic masses
give rise to magnetic anomalies with longer wavelengths and longer, less
steep gradients. In particular, the horizontal length of the steepest
gradient of an anomaly is a measure of its depth of burial (distance
from the aircraft). It can be easily seen that the central portions of
the southern five profiles (lines 35 to 39) are much smoother and flatter
than the remaining profiles and that these smooth profiles are the only
40
lines crossing any substantial thickness of the Oligo-Miocene sediments.
Lines 35 to 39 have therefore been examined for qualitative evidence
bearing on the interpretation of the gravity map. The features noted
will be discussed from east to west across the project area. Check
points can be located on figure 31. .
At the extreme east end of lines 38 and 39 near checkpoints 37 and
41, respectively, the data indicate basement rocks gradually approach
very near the surface about 3 km east of Salinas. This result agrees
with the gravity data which indicate the east termination of the coastal
plain at the same approximate location. The contact here is probably
not a fault.
Line 37 crosses the north border of the Middle Tertiary sediments
about 1 km west of checkpoint 08 at a point which is 6 km west of Salinas,
The steep magnetic gradient implies a major fault here, with an abrupt
change from deeply buried basement on the west to shallow basement east
of the fault. A similar fault has already been inferred at this location
from the gravity data.
The gravity high south of Santa Isabel is traversed by line 38, in
the vicinity of checkpoint 30, and by line 39, near checkpoint 46. There
is reasonably good evidence on line 38 that basement is significantly
more shallow over this gravity anomaly than on the adjacent portions of
the profile. The data of line 39 are not conclusive although a small
local magnetic high is present at checkpoint 46.
41
The gravity high 2 km west of Pastille is crossed by line 37 between
checkpoints 22 and a point 4 km to the east. Again a broad magnetic anomaly
indicates relatively shallow depth to magnetic rocks and confirms the
interpretation from gravity data that basement is relatively near the
surface at the gravity high.
Various magnetic anomalies in the central portions of lines 35, 36,
38, and 39 are caused by man-made structures on the surface of the ground.
Lines 35 and 36 cross the city of Ponce near checkpoints 65 and 24, re
spectively, and the magnetic effects are evident- on the profiles. The
large anomaly on line 38 3 km west of checkpoint 22 is caused by some
industrial effect at the Playa de Ponce docks. Lastly, the anomaly on
line 39, halfway between location points 51 and 59 is caused by flying
over a ship.
A northeast-trending gravity high parallels the northwest shore of
Bahia de Guayanilla. Lines 35 and 36 cross this gravity feature at
points 2 km west of checkpoint 74 and 3 km east of checkpoint 12, re
spectively. At these profile locations are various shallow-depth magnetic
anomalies. Although a few of these magnetic features may be industrial,
it is felt that some of the anomalies are generated by magnetic basement
rocks which are here less deeply buried than on adjacent portions of the
profiles. Again both the gravity and magnetic data suggest relatively
shallow basement depth at this location.
The inliers of basement rocks west of Central San Francisco are
crossed by line 37 where very shallow-depth magnetic anomalies occur
between checkpoint 46 and a point 5 km to the west. The shallow-depth
anomalies thus extend about 1 km east of the mapped exposure of serpen-
tinite (figure 14).
42
Conclusions and Recommendations
The objectives of the present gravity survey were to determine the
general configuration of the basement surface beneath the Tertiary coastal
plain of the south coast and to locate related structures within the over
lying sediments which might be favorable for the accumulation of petroleum
These objectives have been substantially attained and the seismic and
magnetic data confirm the gravity interpretation. It is clear from
the preceding discussions that the gravity method in this area will in
general only locate the larger structures. More detailed gravity surveys
within small portions of the project area will certainly locate minor
gravity features not delineated on the accompanying gravity map (figure
but the interpretation of these minor features may be difficult and
speculative because of the lack of subsurface information and the absence
of adequate density data, particularly from the nearr-surface alluvial
deposits. The uncertainty concerning the regional gradient across the
project area is also a serious difficulty that could possibly be ovei-come
by analysis of derivative or residual maps of more detailed gravity data.
If further information is desired concerning the structure and
basement configuration of the offshore portions of the coastal plain,
it is clear from the pr esent survey that an underwater gravity survey
will provide useful information. Further seismic data, both on land and
offshore, are also needed to determine structures above and below the
unconformity which appears to exist within the Oligo-Miocene rocks.
43
References.
Briggs, R. P., 1961, Geology of Kewanee Interamerican Oil Company
test well number 4CPR, northern Puerto Rico, in Oil and gas
possibilities of northern Puerto Rico: San Juan, Puerto Rico
Mining Comm., p. 1-23.
1964, Provisional geologic map of Puerto Rico and adjacent
islands: U.S. Geol. Survey Misc. Geol. Inv. Map 1-392.
Bromery, R. W., and Griscom, Andrew, 1964, A gravity survey in the
Mayaguez area of southwest Puerto Rico, in C. A. Burk, ed., A
study of serpentinite, the AMSOC core hole near Mayaguez, Puerto
Rico: Natl. Acad. Sci. - Natl. Research Council Publ. 1188,
p. 61-74.
Denning, W. H., 1948, Report on seismograph survey of Puerto Rico with
principal reference to the south coastal area: United Geophysical
Company, Inc., for Puerto Rico Industrial Development Company, 17 p,
Donnally, C. J., 1958, Santa Isabel area of Puerto Rico for Maritime
Oil Company by Donnally Geophysical Company, 5 p.
Glover, Lynn, 3d, 1961, Preliminary report on the geology of the Coamo
quadrangle, Puerto Rico: U.S. Geol. Survey Misc. Geol. Inv. Map
1-335.
Glover, Lynn, 3d, and Mattson, P. H., 1960, Successive thrust and trans-
current faulting during the early Tertiary in south-central Puerto
Rico: Art. 166, in U.S. Geol. Survey Prof. Paper 400-B, p. B363-
B365.
44
Grossman, I. G., 1962, Stratigraphy and hydrology of the Juana Diaz
Formation in the Yauco area, Puerto Rico: Art. 137 in U.S. Geol.
Survey Prof. Paper 450-D, p. D62-63.
____1963, Geology of the Guanica-Guayanilla Bay area, southwestern
Puerto Rico: Art. 29 jLn U.S. Geol. Survey Prof. Paper 475-B,
p. B114-B116.
Mattson, P. H., 1960, Geology of the Mayaguez area, Puerto Rico: Geol.
Soc. America Bull., v. 71, no. 3, p. 319-362.
Ming, R. E., 1958, Geological Report, oil and gas possibilities of the
Santa Isabel prospect, Puerto Rico: for the Maritime Oil Company,
11 p.
Pessagno, E. A., Jr., 1960a, Geology of Ponce-Coamo Area, Puerto Rico:
Ph.D. Thesis, Princeton University.
________1960b, Stratigraphy and micropaleontology of the Cretaceous and
lower Tertiary of Puerto Rico: Micropaleontology, v. 6, no. 1,
p. 87-110. Seiglie, G. A., and Bermudez^ P. J., 1969, Informe preliminar sobre los
foraminiferos del Terciario del sur de Puerto Rico: Caribbean
Jour. Sci., v. 9, no. 1-2, p. 67.
Shurbet, G. L., and Ewing, Maurice, 1956, Gravity reconnaissance survey
of Puerto Rico: Geol. Soc. America Bull., v. 67, no. 4, p. 511-534.
Slodowski, T. R., 1956, Geology of the Yauco Area, Puerto Rico: Ph.D.
Thesis, Princeton University.
Swick, C. H., 1942, Pendulum gravity measurements and isostatic reduc
tions: U.S. Coast & Geodetic Survey, Spec. Pub. No. 232, 82 p.
U.S. Geological Survey, 1964, Geological Survey Research, 1964: U.S.
Geol. Survey Prof. Paper 501-A, p. A120.
Zapp, A. D., Bergquist, H. R., and Thomas, C. R., 1948, Tertiary geology
of the coastal plains of Puerto Rico: U.S. Geol. Survey Oil & Gas
Inv. Prelim. Map 85.
45
Explanation and footnotes
to Table 4
U.S.G.S. GRAVITY REDUCTION PROGRAM
First line of printout
63 The year of the gravity survey, 1963
DOWNTOWN PONCE - The U.S.C.&G.S. Ponce pendulum
base as reoccupied during the survey (see
description in report).
GBV 978627.84 - Gravity base value in mgal
MSV .10445 or .53876 - Meter scale value is
.10445 x 10 mgal/dial division for the
LaCoste and Romberg Model G gravimeter and
.53876 mgal/dial division for the Worden
gravimeter.
Dl 2.67 - Density used to compute BA1
D2 2.27 - Density used to compute BA2
BY WLR - Submitted by William L. Rambo
Input data
STA - Station number
LAT - Latitude in degrees and minutes (to accuracy of1/100 minute)
LONG- Longitude in degrees and minutes
E - Elevation in feet
MG/OG- Observed gravity in meter scale divisions relative
to the GBV (gravity base value) shown at the top
of listing.
Output data
OG - Observed gravity in mgal minus 978000.00 mgal
computed from the MSV (meter scale value) relative
to GBV as follows:
OG - GBV » (MSV) (MG)
Output data cont'd
FTH - Theoretical gravity at sea level at the station
latitude 4> computed according to the International
Gravity Formula:
FTH - 978049 [1 + .0052884 sina *
- .0000059 sin3 2*] mgal
The actual form used by the datatron is as follows:
978049 [1 + sin3 * (.0052648 + .0000236 sin3 *]
FAA - Free-air anomaly computed as follows:
FAA « OG - FTH + FAC
where free air correction,
FAC (.09411 - .000134 sina OE - .0067 (ExlO"8 )
When E, elevation, is expressed in feet, FAC and
FAA will be in mgal.
BA1 - Simple Bouguer Anomaly
BA « FAA - 0.01276 p ± E
where p. is the assumed rock density
E is the elevation in feet
CC - Curvature correction computed to an accuracy of
0.1 mgal by the approximation
1.74 sin ~ , E < 14,000 feet
TC - Terrain correction: Input data computed for p « 2.67
Then p.TC i 2767- TC
MT - Modified tidal correction. This is the residual
tidal correction not taken into account by the
daily meter drift curves.
CBA - Complete Bouguer Anomaly,
» BA, - CC 4- T
Footnotes
Page 2
1. Correction of -0.1 SD applied to CBA
2. Correction of +0.2 SD applied to CBA
Page 3
1. Error in sign of MG/OG. CBA only is corrected
Page 4
1. Error in elevation. Should read 527*6 feet.CBA only is corrected.
2. Error in elevation. Should read 575.8 feet.CBA only is corrected.
Page 6
1. Correction of +0.2 SD applied to CBA
2. " " +0.1 SD " " "
3. " " +0.3 SD " " "
4. " " -0.1 SD " " "
Page 7
1. Correction of +0.2 SD applied to CBA
2. " " +0.3 SD " " "
Page 12
1. Latitude error. Should read 17 57.88, FTH=0539.05, FAA«93.93, BA1-93.85, CBA is"corrected.
2. Elevation error. Should read 352.7 'feet, FAA«130.06, BA1-118.04, CBA is corrected.
Page 14
1. Error in sign of MG/OG.OG=641.37, FAA-104.48, BA1-103.19, CBA is corrected.
Page 14 cont 1 d
2. Error in sign of MG/OG.OG=636.21, FAA=104.80, BA1-100.75 CBA is corrected.
3. Error in sign of MG/OG.OG-634.65, FAA=115.36, BA1-106.31, CBA is corrected.
4. Error in sign of MG/OG.06=640.01, FAA-110.01, BA1-105.24, CBA is corrected.
Table 4
Principal facts
for
the
gravity data
from th
e so
uth
coas
t of
Puerto Rico
PUERTORiCQ
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