Publication of the International Association of Sedimentologists,
21, pp. 3–20.
Saller, A. H., 1984. Petrological and geochemical constraints on the
origin of subsurface dolomite, Enewetak Atoll: an example of
dolomitization by normal seawater. Geology, 12, 217–220.
Schlanger, S. O., 1963. Subsurface geology of Eniwetok Atoll.
U.S. Geological Survey Professional Papers 260, -BB:
pp. 991–1066.
Shinn, E. A., Ginsburg, R. N., and Lloyd, R. M., 1965. Recent
supratidal dolomite from Andros Island, Bahamas. In Pray,
L. C., and Murray, R. C. (eds.), Dolomitization and Limestone
Diagenesis: A Symposium. Society of Economic
Palaeontologists and Mineralogists, Special Publications 13,
pp. 112–123.
Skeats, E. W., 1903. The chemical composition of limestones from
upraised coral islands, with notes on their microscopial structures. Bulletin Museum Comparative Zoology, Harvard Collection, Vol. 42, pp. 53–126.
Skeats, E. W., 1905. The chemical and mineralogical evidence as to
the origin of the dolomites of Southern Tyrol. Quarterly Journal
Geological Society of London, 61, 97–141.
Strasser, A., and Strohmenger, C., 1997. Pleistocene coral reefs,
southern Sinai, Egypt: response to tectonics, sea-level and climate. Sedimentology, 44, 537–558.
Suzuki, Y., Iryu, Y., Inagaki, S., Yamada, T., Aizawa, S., and Budd,
D. A., 2005. Origin of atoll dolomites distinguished by geochemistry and crystal chemistry: Kita-daito-jima, northern
Philippine Sea. Sedimentary Geology, 183, 181–202.
Swart, P. K., 1993. The formation of dolomite in sediments from
the continental margin of northeastern Australia. In Proceedings
of the Ocean Drilling Program, Scientific Results, Vol. 133,
pp. 513–523.
Trichet, J., Repellin, P., and Oustriere, P., 1984. Stratigraphy and
subsidence of the Mururoa Atoll (French Polynesia). Marine
Geology, 56, 241–257.
Tucker, M. E., and Wright, V. P., 1991. Carbonate Sedimentology.
Oxford: Blackwell.
Vahrenkamp, V. C., and Swart, P. K., 1994. Late Cenozoic dolomites of the Bahamas: metastable analogues for the genesis of
ancient platform dolomites. In Purser, B., Tucker, M., and
Zenger, D. (eds.), Dolomites, a Volume in Honour of Dolomieu.
Special Publication of the International Association of Sedimentologists, 21, pp. 133–154.
Van Tuyl, F. M., 1916. The origin of dolomite. Iowa Geological
Survey Annual Report, 25, 251–421.
Vasconcelos, C., and McKenzie, J. A., 1997. Microbial mediation of
modern dolomite precipitation and diagenesis under anoxic conditions (Lagoa Vermelha, Rio de Janiero, brazil). Journal of Sedimentary Research, 67, 378–390.
Vasconcelos, C., Mckenzie, J. A., Bernasconi, S., Grujic, D., and
Tine, A. J., 1995. Microbial mediation as a possible mechanism
for natural dolomite formation at low temperatures. Nature, 377,
220–222.
Warren, J., 2000. Dolomite occurrences, evolution and
economically important associations. Earth Science Reviews,
52, 1–81.
Warthmann, R., van Lith, Y., Vasconcelos, C., McKenzie, J. A., and
Karoff, A. M., 2000. Bacterially induced dolomite precipitation
in anoxic culture experiments. Geology, 28, 1091–1094.
Webster, J. M., and Davies, P. J., 2003. Coral variation in two deep
drill cores: significance for the Pleistocene development of the
Great Barrier Reef. Sedimentary Geology, 159, 61–80.
Wheeler, C., and Aharon, P., 1997. Geology and Hydrology of Carbonate Islands In Vacher, H. L., and Quinn, T. M. (eds.), Developments in Sedimentology, 54, pp. 537–564.
Wright, D. T., and Wacey, D., 2004. Sedimentary dolomite –
a reality check. In Braithwaite, C. J. R., Rizzi, G., and Darke,
G. (eds.), The Geometry and Petrogenesis of dolomite Hydrocarbon Reservoirs. Geological Society Special Publication, 235,
pp. 65–74.
Cross-references
Atolls
Coral Reef, Definition
Diagenesis
Porosity Variability in Limestone Sequences
DOUBLE AND TRIPLE REEF FRONTS
David Hopley
James Cook University, Townsville, QLD, Australia
Definition
The reef front is the windward margin of a coral reef with
multiple fronts produced by narrower and younger sections of reef flat to windward of the main front.
The windward side of most reefs is formed by a straight
edge or “hard line.” Occasionally, however, there may be
a second or third line of reefs separated from the main reef
by linear lagoons up to 300 m wide and 10–30 m deep.
Such features have been described in New Caledonia
(Guilcher, 1965; Chevalier, 1973; Battistini et al., 1975),
Mayotte (Battistini et al., 1975), and Australia’s Great
Barrier Reef (Hopley et al., 2007). It is suspected that
other reefs, especially shelf reef systems may contain similar features.
Where double barriers occur, the outer reef invariably
appears younger and may be still slightly submerged
(see for example the double barrier of S.E. New Caledonia
shown in Figure 5, Battistini et al., 1975). This has
resulted in the suggestion that the outer barrier(s) grew
from deeper foundations possibly added to the reef
front as terraces during the last glacial interstadials or
the Holocene transgression. The examples of the Great
Barrier Reef suggest that such terraces are typically at
20–30 m depth while the Pleistocene reef to which they
are attached is only 10–15 m below modern sea level.
Contrasting rates of growth may have resulted: the reef
growing from the terrace lagging behind sea level rises
as a “catch up” reef while the main reef growing from
the more extensive Pleistocene foundations would have
adopted a “keep up” strategy, the result leading to
a mature reef (crescentic, lagoonal) and an immature
secondary reef front.
The double reef front on Gable Reef (20
48
0 S)
(Figure 1) has been examined in detail (Hopley et al.,
2007, Figure 8.13). This Great Barrier Reef site is on the
windward south-eastern rim with the secondary rim
stretching partly across a wide embayment. The depth of
DOUBLE AND TRIPLE REEF FRONTS
325
21, pp. 3–20.
Saller, A. H., 1984. Petrological and geochemical constraints on the
origin of subsurface dolomite, Enewetak Atoll: an example of
dolomitization by normal seawater. Geology, 12, 217–220.
Schlanger, S. O., 1963. Subsurface geology of Eniwetok Atoll.
U.S. Geological Survey Professional Papers 260, -BB:
pp. 991–1066.
Shinn, E. A., Ginsburg, R. N., and Lloyd, R. M., 1965. Recent
supratidal dolomite from Andros Island, Bahamas. In Pray,
L. C., and Murray, R. C. (eds.), Dolomitization and Limestone
Diagenesis: A Symposium. Society of Economic
Palaeontologists and Mineralogists, Special Publications 13,
pp. 112–123.
Skeats, E. W., 1903. The chemical composition of limestones from
upraised coral islands, with notes on their microscopial structures. Bulletin Museum Comparative Zoology, Harvard Collection, Vol. 42, pp. 53–126.
Skeats, E. W., 1905. The chemical and mineralogical evidence as to
the origin of the dolomites of Southern Tyrol. Quarterly Journal
Geological Society of London, 61, 97–141.
Strasser, A., and Strohmenger, C., 1997. Pleistocene coral reefs,
southern Sinai, Egypt: response to tectonics, sea-level and climate. Sedimentology, 44, 537–558.
Suzuki, Y., Iryu, Y., Inagaki, S., Yamada, T., Aizawa, S., and Budd,
D. A., 2005. Origin of atoll dolomites distinguished by geochemistry and crystal chemistry: Kita-daito-jima, northern
Philippine Sea. Sedimentary Geology, 183, 181–202.
Swart, P. K., 1993. The formation of dolomite in sediments from
the continental margin of northeastern Australia. In Proceedings
of the Ocean Drilling Program, Scientific Results, Vol. 133,
pp. 513–523.
Trichet, J., Repellin, P., and Oustriere, P., 1984. Stratigraphy and
subsidence of the Mururoa Atoll (French Polynesia). Marine
Geology, 56, 241–257.
Tucker, M. E., and Wright, V. P., 1991. Carbonate Sedimentology.
Oxford: Blackwell.
Vahrenkamp, V. C., and Swart, P. K., 1994. Late Cenozoic dolomites of the Bahamas: metastable analogues for the genesis of
ancient platform dolomites. In Purser, B., Tucker, M., and
Zenger, D. (eds.), Dolomites, a Volume in Honour of Dolomieu.
Special Publication of the International Association of Sedimentologists, 21, pp. 133–154.
Van Tuyl, F. M., 1916. The origin of dolomite. Iowa Geological
Survey Annual Report, 25, 251–421.
Vasconcelos, C., and McKenzie, J. A., 1997. Microbial mediation of
modern dolomite precipitation and diagenesis under anoxic conditions (Lagoa Vermelha, Rio de Janiero, brazil). Journal of Sedimentary Research, 67, 378–390.
Vasconcelos, C., Mckenzie, J. A., Bernasconi, S., Grujic, D., and
Tine, A. J., 1995. Microbial mediation as a possible mechanism
for natural dolomite formation at low temperatures. Nature, 377,
220–222.
Warren, J., 2000. Dolomite occurrences, evolution and
economically important associations. Earth Science Reviews,
52, 1–81.
Warthmann, R., van Lith, Y., Vasconcelos, C., McKenzie, J. A., and
Karoff, A. M., 2000. Bacterially induced dolomite precipitation
in anoxic culture experiments. Geology, 28, 1091–1094.
Webster, J. M., and Davies, P. J., 2003. Coral variation in two deep
drill cores: significance for the Pleistocene development of the
Great Barrier Reef. Sedimentary Geology, 159, 61–80.
Wheeler, C., and Aharon, P., 1997. Geology and Hydrology of Carbonate Islands In Vacher, H. L., and Quinn, T. M. (eds.), Developments in Sedimentology, 54, pp. 537–564.
Wright, D. T., and Wacey, D., 2004. Sedimentary dolomite –
a reality check. In Braithwaite, C. J. R., Rizzi, G., and Darke,
G. (eds.), The Geometry and Petrogenesis of dolomite Hydrocarbon Reservoirs. Geological Society Special Publication, 235,
pp. 65–74.
Cross-references
Atolls
Coral Reef, Definition
Diagenesis
Porosity Variability in Limestone Sequences
DOUBLE AND TRIPLE REEF FRONTS
David Hopley
James Cook University, Townsville, QLD, Australia
Definition
The reef front is the windward margin of a coral reef with
multiple fronts produced by narrower and younger sections of reef flat to windward of the main front.
The windward side of most reefs is formed by a straight
edge or “hard line.” Occasionally, however, there may be
a second or third line of reefs separated from the main reef
by linear lagoons up to 300 m wide and 10–30 m deep.
Such features have been described in New Caledonia
(Guilcher, 1965; Chevalier, 1973; Battistini et al., 1975),
Mayotte (Battistini et al., 1975), and Australia’s Great
Barrier Reef (Hopley et al., 2007). It is suspected that
other reefs, especially shelf reef systems may contain similar features.
Where double barriers occur, the outer reef invariably
appears younger and may be still slightly submerged
(see for example the double barrier of S.E. New Caledonia
shown in Figure 5, Battistini et al., 1975). This has
resulted in the suggestion that the outer barrier(s) grew
from deeper foundations possibly added to the reef
front as terraces during the last glacial interstadials or
the Holocene transgression. The examples of the Great
Barrier Reef suggest that such terraces are typically at
20–30 m depth while the Pleistocene reef to which they
are attached is only 10–15 m below modern sea level.
Contrasting rates of growth may have resulted: the reef
growing from the terrace lagging behind sea level rises
as a “catch up” reef while the main reef growing from
the more extensive Pleistocene foundations would have
adopted a “keep up” strategy, the result leading to
a mature reef (crescentic, lagoonal) and an immature
secondary reef front.
The double reef front on Gable Reef (20
48
0 S)
(Figure 1) has been examined in detail (Hopley et al.,
2007, Figure 8.13). This Great Barrier Reef site is on the
windward south-eastern rim with the secondary rim
stretching partly across a wide embayment. The depth of
DOUBLE AND TRIPLE REEF FRONTS
325