1Geology of Isla de Mona, Puerto Rico



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1Geology of Isla de Mona, Puerto Rico

By Edward Frank, Carol Wicks, John Mylroie, Joseph Troester, E. Calvin Alexander, Jr, and James Carew.


Abstract:

Isla de Mona is a carbonate island located in the Mona Passage 68 kilometers west of Puerto Rico. The island is 12 kilometers by 5 kilometers, has an area of 55 km2, and has been tectonically uplifted to form a raised flat-topped platform or meseta. The meseta tilts gently to the south and is bounded by near vertical cliffs on all sides. These cliffs range in height from 80 meters above sea level on the north to twenty meters above sea level on the southern coast. Along the southwestern and western side of the island a 3 to 6 meter high Pleistocene fossil reef abuts the base of the cliff to form a narrow coastal plain. The meseta itself consists of two Mio-Pliocene carbonate units, the lower Isla de Mona Dolomite and the upper Lirio Limestone. Numerous karst features are found on the island, including a series of flank margin caves, primarily developed at the Lirio Limestone/Isla de Mona Dolomite contact, that literally ring the periphery of the island.


Introduction

Isla de Mona is a tectonically uplifted Mio-Pliocene carbonate island located in the Mona Passage approximately half way between Puerto Rico and Hispanola (Figure 1). The kidney-shaped island is 12 kilometers long and 5 kilometers wide and covers 55 km2 (Peck et al., 1981). The bulk of the island forms a flat-topped, raised platform, or meseta, that dips gently to the south (Figure 1). This meseta is bounded on all sides by vertical to near vertical cliffs. (The Puerto Ricans refer to the flat-topped, raised platform of Isla de Mona as a meseta. For consistency, the authors of papers in this volume will also use meseta, however, it should not be confused with the geographic definition of the term). Along the north coast the cliff drops vertically from a maximum elevation of 80 meters to a depth of at least 30 meters below sea level. Along the southern and western margins of the island a Pleistocene fossil reef abuts the base of the 20 to 30 meter-high cliffs to form a 3 to 6 meter high coastal flat. This reef flat is generally narrow with a maximum width of 1 kilometer in the Piedra del Carabinero area of the southern coast. Offshore a modern coral reef parallels the shore from Punta Este, around the southern coast, and northward almost to Punta el Capitan along the western coast of the island. This reef is separated from shore by a shallow lagoon that ranges from a few meters to a few hundred meters wide. A small sister island, Monito, is located 5 kilometers northwest. It is similar in description but occupies only 0.17 km2 of area (Peck et al., 1981) (Figure 2).


Tectonics

The major tectonic features of the region are the Puerto Rico Trench to the north, the Muertos Trough to the south and southwest, the Anegada Passage to the southeast, and the Mona Canyon running north-south between Puerto Rico and Hispaniola (Figure 3). The Puerto Rico Trench marks the boundary between the Caribbean and North American plates. Because it is not completely linear, portions of the boundary of the Caribbean plate are undergoing subduction, while in other areas the relative motion results in strike-slip faults. Compression along the Muertos Trough decreases gradually eastward, ultimately to be replaced by extension in Anegada Passage. Northwest of Puerto Rico an obvious structural break occurs along Mona Canyon. However no obvious structural or seismic continuity links Mona Canyon to the Muertos Trough to the south. One possibility is that Puerto Rico and eastern Hispaniola are both undergoing counterclockwise movement as independent or semi-independent blocks. The extensional forces that produced Mona Canyon are a result of the relative movement between them (Masson and Scanlon, 1991).

On Isla de Mona itself there are a number of tectonic features expressed. A series of low amplitude southward plunging anticlines/synclines cross the island. The island itself has undergone tectonic uplift since deposition and is generally tilted to the south at 5-10 meters per kilometer (0.3 to 0.6 degrees dip). A large fault (Figure 2) extends inward from the north shore through the Bajura de los Cerezos and terminates in the south central portion of the meseta (Briggs and Seiders, 1973).
Stratigraphy

Isla de Mona is dominated by a carbonate meseta which consists of two units, the Isla de Mona Dolomite and the Lirio Limestone (Figure 2). Kaye (1959) placed the age of the Lirio Limestone as Middle Miocene based upon a limited foraminifera assemblage identified in samples. More recent work by Gonzales et al. (1994) suggest a younger date of late Miocene to early Pliocene age for the major carbonate units of the island based upon overall coral assemblages.



The Isla de Mona Dolomite is a pale tan, very finely crystalline, calcitic dolomite. It is thick to massively bedded, and locally cross bedded (Quinlan, 1974). The maximum exposure above sea level is 80 meters near Cabo Noroeste (Briggs, 1974). The dolomite has a limited surface area of outcrop, however volumetrically it makes up the largest portion of the island and outcrops extensively along the near vertical cliff faces surrounding the island and in the Bajura los Cerezos area in the central portion of the island.

The Lirio Limestone overlies the Mona Dolomite and forms the cap on the island. It is a pale tan, finely crystalline limestone. The maximum exposed thickness is 40 meters near Playa Sardinia, but averages only 10 to 15 meters thick along the cliff tops. The limestone bedding ranges from 2 to 5 meters in thickness, with cross beds locally up to 2 to 3 centimeters thick. The Lirio Limestone is moderately fossiliferous, with accumulations of large coral heads and patch reefs near Cueva del Capitan and Cuevas del Centro (Briggs, 1974). This unit is extensively karstified with caves, karren, sinkholes, pits, and enlarged joints present across the plateau surface.

Ruiz (1993) did detailed petrographic work on rock samples collected from the island. He provides a description of the origin of the carbonate units (p. 70-71) as follows: "The carbonate build-up of Isla de Mona is the result of the development of a barrier reef of middle Miocene to earliest Pliocene age. Four reef facies have been identified in the Tertiary deposits of the island. Fore-reef deposits characterized by muds, pelagic foraminifera, and steeply dipping strata are present on the southwestern cliffs. A reef is exposed along the southeastern coast as well as in the western tip of the island. A transition between reef-flat and back-reef deposits is present to the north of the reef. Lagoon deposits composed of pelleted muds, benthic foraminifera, and coralline algae, makes up the bulk of the island's carbonates. Scattered patch-reefs are locally developed in the lagoon facies." Ruiz treats both units as part of a single reef complex.

The nature of the contact between the Lirio Limestone and the Isla de Mona Dolomite has been the subject of much speculation. In the cliffs along the eastern and northern shores of the island there is a marked difference in the coloration of the rock units above and below the major band of cave development. Kaye (1959) found that the unit above the band was darker in color and a relatively pure limestone while the unit below the cave band was lighter in color and was found to be dolomitic limestone or dolomite. An apparent angular unconformity was also noted at the contact between the upper darker-colored rocks and the lower lighter-colored rocks in the cliffs around Punta Este. Kaye (1959) defined the upper unit which forms a thin cap over much of the island as the Lirio Limestone and the lower unit which makes up the bulk of the island as the Isla Mona Limestone.

Briggs and Seiders (1972) redefined these units so that the entire exposed cliff near Punta Arenas was reassigned to the Lirio Limestone and the Isla Mona Limestone was renamed the Isla de Mona Dolomite. Briggs (1974) suggested as an alternative interpretation that the contacts between the two unit might be essentially conformable with the apparent angular unconformity simply being large scale crossbeds. He also notes that where the contact is exposed in the cliffs along the western and southeastern shores of the island, examination from a distance gives the impression that the lower few meters of the Lirio Limestone grade laterally into the upper Isla de Mona Dolomite. Ruiz (1993) does not directly address the question of the nature of the contact between the Lirio Limestone and the Isla de Mona Dolomite. Gonzales et al. (1994) found the Lirio Limestone/Isla de Mona Dolomite contact to be conformable. The lithology at the base of the Lirio Limestone is dolomitic limestone and gradually changes upward into almost pure limestone at the top of the unit. The dolomitized section extends several meters above the unit contacts.

The Pleistocene-aged reef tracts composed primarily of a mixed head-coral facies overlain by an extensive Acropora palmata reef-crest facies extend along 14 kilometers of the southern and western coasts of the island (Figure 2). These deposits are found at elevations of up to 5 meters above sea level, and at distances of several hundred meters from the present day shoreline (Taggart, 1993).

Radiometric dating using the 230Th/234U method have shown these reefs to have been active from 107 to 128 thousand years ago (Taggart, 1993). The presence of these last interglacial deposits at positions between sea level and 6 m elevation indicate there has been no tectonic movement of the Mona platform for over 100,000 years.

Locally these reef tracts are capped by beach sands. Boulders of Isla de Mona Dolomite and Lirio Limestone have fallen from the cliffs and are located sporadically at the base of the cliffs surrounding the island. Large coral boulders up to 5 meters across have been torn from the Holocene reefs and deposited on top of the late Pleistocene coastal flats in the southwestern portion of the island within the last 3,000 years (Taggart et al., 1993).

Karst Development

A variety of karst features are found on the island. The most prominent of these are a series of caves that ring the periphery of the island. The majority of these caves are developed at the Lirio Limestone/Isla de Mona Dolomite contact, whereas others are independent of this formational boundary. The caves are flank margin caves and range in size from a meter or less across to caves containing series of large interconnected rooms that extend more than 1 kilometer. Floor areas of some individual caves and cave systems are in excess of 150,000 m2. The caves are all restricted to the edge of the island with a maximum inward penetration of 240 meters from the cliff face (Frank, 1993; Mylroie et al., 1995, Frank et al., this volume) .

Another significant karst feature is Bajura de los Cerezos, a closed, internally drained, depression in the center of the island developed along a fault line. Other important karst features include: (1) Cuevas del Centro, a series of large nested sinkholes; (2) Los Corrales de los Indios, a dissolutional valley formed along a fracture; (3) Camino de los Cerezos pit area, an area containing a large number of vertical shafts; and (4) the surface of the meseta has been etched by dissolution into small-scale pits.

References:


Briggs, R. P., 1974, Economic geology of the Isla de Mona quadrangle, Puerto Rico: U. S. Geological Survey, Open File Report 74-226, 116 p.
Briggs, R. P. and Seiders, V. M., 1972, Geologic map of the Isla de Mona quadrangle, Puerto Rico: U. S. Geological Survey Miscellaneous Geological Investigations, Map I-718, 1:20,00.
Cintron, B., and Rogers, L., 1991, Plant communities of Mona Island: Acta Cientifica; Asiciacon de Maestros de Ciencia de Puerto 5: 10-64.
Frank, E. F., 1993, Aspects of karst development and speleogenesis, Isla de Mona, Puerto Rico: An snalogue for Pleistocene speleogenesis in the Bahamas: Master of Science Thesis, Department of Geology and Geography, Mississippi State University, 288 p.
Gonzalez, L. A., Ruiz, H., and Monell, V., 1990, Digenesis of Isla Mona, Puerto Rico [abs]: American Association of Petroleum Geologists Bulletin 74: 663-664.
Gonzales, L. A., Ruiz, H. A., Budd, A. F., and Monell, V., 1994, A late Miocene platform margin barrier reef on Isla de Mona, Puerto Rico, in Jordan, C., Colgan, M., and Esteban, M., eds., Miocene Reefs: A Global Comparison: Springer Verlag, 19 ms pages, 8 figures, 1 table.
Kaye, C. A., 1959, Geology of Isla Mona, Puerto Rico, and notes on the age of the Mona Passage: U. S. Geological Survey, Professional Paper 317C, p 141-178.
Martinez, M.I., Troester, J.W., and Richards, R.T., 1995. Surface electromagnetic geophysical exploration of the ground-water resources of Isla de Mona, Puerto Rico, a Caribbean carbonate island: Carbonates and Evaporites 10: .
Masson, D. G. and Scanlon, K. M., 1991, The neotectonic setting of Puerto Rico: Geological Society of America Bulletin 103: 144-154.
Mylroie, J. E., Panuska, B. C., Carew, J. L., Frank, E. F., Taggart, B. E., Troester, J. W., and Carrasquillo, R., 1995, Development of flank margin caves on San Salvador Island, Bahamas and Isla de Mona, Puerto Rico, in Boardman, M., ed., Proceedings of the seventh symposium on the geology of the Bahamas: June 16 - 20, 1994, Bahamian Field Station, San Salvador, Bahamas, p. 49-81.
Peck, S. B., and Kukalova-Peck, J., 1981, The subterranean fauna and conservation of Mona Island, Puerto Rico: National Speleological Society Bulletin. 43: 59-68.
Quinlan, J. F., 1974, Preliminary exploration and evaluation of the caves of Mona Island, including a description of origin: U. S. National Park Service, unpublished administrative report, 33 p.
Richards, R. T., Troester, J.W., and Mart¤ćnez, M.I., 1995. A comparison of electromagnetic techniques used in a reconnaissance of ground-water resources under the coastal plain of Isla de Mona, Puerto Rico: The Symposium on the Applications of Geophysics to Environmental and Engineering Problems (SAGEEP'95) proceedings, Orlando, Florida, 251-260.
Ruiz, H. M., 1993, Sedimentology and diagenesis of Isla de Mona, Puerto Rico: Master of Science. Thesis, University of Iowa, Iowa City, 86 p.
Ruiz, H., Gonzalez, L. A., and Budd, A. F., 1991, Sedimentology and diagenesis of Miocene Lirio Limestone, Isla de Mona, Puerto Rico [abs]: American Association of Petroleum Geologists Bulletin 75: 664-665.
Taggart, B. E., 1993, Tectonic and eustatic correlations of radiometrically dated marine terraces in northwest Puerto Rico and Isla de Mona, Puerto Rico: unpublished PhD. dissertation, Department of Marine Sciences, University of Puerto Rico, Mayaguez, 252 p.
Taggart, B.E., Lundberg, J.I., Carew, J.L., and Mylroie, J.E., 1993, Holocene reef-rock boulders on Isla de Mona, Puerto Rico: Transported by a hurricane or seismic sea wave: : Geological Society of America Annual Meeting Abstracts with Program 25: 61.
List of Figures:
Figure 1: North shore of Isla de Mona showing 70 meter high cliffs and flat surface of the mesata or raised platform surface.
Figure 2: General geologic map and cross section of Isla de Mona, Puerto Rico. Major topographic features are marked. Adapted from Kaye (1959) and Briggs and Seiders (1972).
Figure 3: Regional tectonics of the Isla de Mona area showing major structural features and relative plate motions. Adapted from Mason and Scanlon (1991).








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