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

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gravity data

from th

e so

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t of

Puerto Rico

PUERTORiCQ

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