View allAll Photos Tagged lithics
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= to the right in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= to the right in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
The soft and gentle daylily lays its head against a cool granite pillow in respite from the day’s heat…
We cruised slowly around the Island for a while, watching the seals sunning themselves upon the rocks, and climbing lithely out of the water - or tumbling back in at will.
The Nineteenth Spirit is Sallosi (or Saleosi). She is a Great and Mighty Duchess, and appears in the form of a gallant and most beautiful Athenian Woman of an Amazon, whose body is lithe and gymnastic, whom will be dressed as an ancient Greek Hoplite of a soldier. She will sometimes be seen within ones Visions to be riding upon a Crocodile, which will be the arousal of her Evoked sexual energy caressing ones Reptilian-Brain-Stem. Upon her head she will be wearing a Ducal crown of a crested Hoplite helmet. She is very peacable and most wise in the Chess-Game of Love whose battles she always wins for her Master for she causes the Love of Women to be attracted to Men, and of Men to Women, wherefore she attracts those Women, which her Master desires to become as his alone of Lovers while she to eradicate his competitors from off the Chessboard. She will only do as her Master bids when she is sexually taken within those Erotic Lucid Dreams of Ancient Greece she will instigate via which she will inform her Master in depth about the Arts of Love, Chess and Poetry. She governs over Thirty Legions of Female Hoplites like unto her self.
THE CHESS GODDESS OF LOVE AND SEX
The Succubus Sallosi is somewhat akin to 'Caissa' who is a mythical Goddess featured in a poem called Caïssa written in 1763 by English poet and philologist Sir William Jones. She is portrayed as an ancient Greek Thracian Dryad.
Jones' work was inspired by the poem Scacchia ludus ("The game of Chess"), written by Italian poet Marco Girolamo Vida in 1510.
Because of her historical connection to the game of Chess, Caissa is traditionally considered the patron Goddess of Chess players. For Chess players, Caissa is often invoked as a source of inspiration or luck, e.g. "Caissa was with me in that game." She is sometimes referred to as a "Chess Muse" for her imagined ability to inspire Chess players to play well.
Caissa is also spelled Caïssa. Caissa is pronounced "ky-EE-suh" or "ky-suh."
Caissa the Goddess of Chess Chess is tantalizing. The game itself; the people drawn to it; the symbolism it evokes; the metaphors, which it inspires.
On one level the Chessboard is the battlefield of life upon which two opposing combatants compete: White against Black; Good against Evil; Positive against Negative, Day against Night, Sun against Moon; Man against Woman. It is also a dynamic interaction between two minds, which converge and fuse into creating dynamic moves, like that of dancers or likened more so to lovers, a thing of beauty, sensual in its nuances and graphic in its uncompromising starkness.
Chess is usually seen to be analogous to War. Yet, the elements of Chess, the interaction between two individuals or two minds: the give and take, the parry and thrust, the intensity and passion, of affinity to boxing and sword fighting has more associative links to that of Sexual Lovemaking. However, Chess and that of its relationship to Love, Romance or Sex, involves the inter-relationship between the two genders (depending of course on ones Sexual orientatation); yet Chess is often thought of as a primarily male-oriented game, while it's inclusion of female players to have once sparked off a rapid reaction from tunnel vision males.
Until the end of the 19th century Women, for the most part, were expected to limit themselves to the artistic or domestic sides of Chess playing, leaving the competitive side to the men. This attitude gave rise to the literary fantasy of powerful Women players, a fantasy, which evolved into the preoccupation with the Sexual and physical attributes of a female Chess player.
This Sexual fantasy first occurred in the early days of Chess (Shatranj) and was expressed in the famous compilation of stories, 1001 Arabian Nights. The story tells of Tawaddud, the Slave-Girl whom excels in many areas including Chess:
when the damsel was playing chess with the expert in presence of the Commander of the Faithful, Harun al-Rashid, whatever move he made was speedily countered by her, till she beat him and he found himself checkmated.
“O professor, I will make a wager with thee on this third game.
I will give thee the queen and the right-hand castle and the left-hand knight; if thou beat me, take my clothes, and if I beat thee, I will take thy clothes.” Replied he, “I agree to this;” and they replaced the pieces, she removing queen, castle and knight. Then said she, “Move, O master.” So he moved, saying to himself, “I cannot but beat her, with such odds,” and planned a combination; but, behold, she moved on, little by little, till she made one of her pawns a queen and pushing up to him pawns and other pieces, to take off his attention, set one in his way and tempted him to take it. Accordingly, he took it and she said to him, “The measure is meted and the loads equally balanced. Eat till thou are over-full; naught shall be thy ruin, O son of Adam, save thy greed. Knowest thou not that I did but tempt thee, that I might finesse thee? See: this is check-mate!” adding, “So doff off thy clothes.” Quoth he, “Leave me my bag-trousers, so Allah repay thee;” and he swore by Allah that he would contend with none, so long as Tawaddud abode in the realm of Baghdad. Then he stripped off his clothes and gave them to her and went away." (Translation by Richard Burton)
Dilaram was the favorite wife of Grand Vizier's Harem. Her husband, Murwadi, had been playing Chess for high stakes and losing badly. He had lost his entire fortune, his possessions and finally all his wives except for Dilaram. He finally used her as stakes for his last chance to gain back some of his losses. But his game looked bad, especially since his opponent would mate him on the next move. Dilaram was, of course, watching the game of her fate closely. She was a much better player than her husband, and actually much better than his adversary. She looked at the position on the board and saw how her husband could win. Since she wasn't allowed to advise him, she clothed her instructions by shouting, "Sacrifice your two rooks, but don't sacrifice me!" Her husband considered her words carefully and found the winning moves.
The story above accompanied a position (called a Mansuba) entitled "Dilaram’s Mate" and was first recorded by Firdewsi at-Tahihal in his book on Chess in the 15th century. It's suspected that the story and problem were first given in the 10th century book, Kitab Ash-Shatranj by the legendary Abu-Bakr Muhammad ben Yahya as-Suli.
The fantasy of the powerful Woman Chess player culminated in the creation of Caïssa, the Goddess of Chess. Caïssa was invented by Sir William Jones, the hyper-polyglot Mathematician in his1763 Latin poem of the same name. In the poem Ares, the God of War, pursued Caïssa, a dryad, with little success. The God of Sport advised Ares to create a game for her to win her over. That game was Chess.
Later writers were less interested in the fantasy and more intent on metaphors and symbols and the game of Love.
Even Shakespeare (1564-1616) incorporated a well known, though minor, Chess scene in The Tempest.
The Tempest: Act Five, Scene One (Ferdinand and Miranda)
The entrance of the Cell opens, and discovers Ferdinand and Miranda playing at Chess.
Miranda: Sweet lord, you play me false.
Ferdinand: No, my dearest love, I would not for the world.
Miranda: Yes, for a score of kingdoms you should wrangle, And I would call it fair play
Miranda and Ferdinand are lovers whose fathers are sworn enemies. Their love, represented in a devious game of chess in the final scene, restores harmony between the two families
A more recent modern interpretation of Shakespeare used Chess as a metaphor for Love:
"CAMBRIDGE UNIVERSITY'S EDINBURGH 2003 SHOW - LOVE'S LABOUR'S LOST AS YOU'VE NEVER SEEN IT BEFORE!
Want to play a game?....
Cambridge University Ariel Society is proud to present their Edinburgh Fringe 2003 Show ‘Love’s Labour’s Lost’. Taken from the Shakespearean script, this production seeks to fully foreground Shakespeare's already self-conscious dramaturgy, and provide an insight into his most enigmatic play.
Set around the concept of a chess game, ‘Love’s Labour’s Lost’ becomes a game of love. The battle of the sexes, the elaborate moves and countermoves of the men and women, and the assumption wrongly made by the women that the courtship is just sport are all heightened by the chessboard setting. Chess appears throughout the script, along with countless other images of games, playing, winning... and losing."
Chaucer (1343-1400) took a rather clever approach; instead of lovers (or simply a man and woman) playing a symbolic game of love, the man plays a game (in a dream) against Fortune and losses his "Queen," his "bliss. (Such is very similar to stories of a man playing against the Devil for his Soul in a symbolic battle of Good versus Evil in the game of Life) This story is related in one of his earliest works, Book of the Duchess:
In reality Chess was played by women in the Middle-Ages, but their participation was usually limited to playing their husbands or those of their betrothed; whereby depictions of women playing at chess with men often symbolized the relationship between the man and the woman.
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= to the left in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= behind the photographer in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
This to me is a lithe young female sea lion as number 22 of 25 drawings in the new 'Detailed Animal Sketches - Back from the BRINK' by Tim Jeffs and caught in a marvellously typical swimming action.
Their status is categorised as 'near threatened' for many reasons however over the last few years there has been an increase in their numbers.
Just one interesting fact this time! Once sold for their meat and fur, their whiskers were also sold at a penny each for use as pipe cleaners!
This one coloured with the sometimes maligned and often overlooked Derwent Procolour pencils which I find quite easy to use.
Name: Chigaru Bomani
Runner name: Anubian and HH
Apparent Age/True Age: 28
Gender: Male
Profession: Combat Decker
~ Appearance ~
Height: 5’10”
Weight: 157
Eyes: Brownish gold
Hair Color: Raven black
Hair Style: Cropped short
Complexion: Slightly pale
Build: lithe
Scars: None visible
Distinguishing Features: Funded by his numerous illegal jobs of hacking into some of the world's most protected companies, Anubian has been able to construct a mobile and armored computer. The physical armor that he wears is shaped in the image of the Egyptian god Anubis. The armor holds his computer and various cyberware.
~ Attributes ~ (12 additional dots)
Intelligence ***
Wits ***
Resolve **
Strength *
Dexterity **
Stamina **
Presence **
Manipulation ***
Composure ***
~ Skills ~ (22 dots)
Academics**
Computer****
Crafts
Investigation**
Medicine
Occult
Politics*
Science
Athletics**
Brawl
Drive
Firearms
Larceny*
Stealth**
Survival**
Weaponry*
Animal Ken
Empathy
Expression
Intimidation
Persuasion**
Socialize*
Streetwise**
Subterfuge
~ Possessions ~
Weapons: Sawed off shotgun
Armor: See the Garb of Anubis
Cybernetics: Chigaru possesses two, four slotted datajacks in the back of his head. Using these jacks, he is able to insert Data cards and memstick into his head to access or store information upon them.
Important Items: Garb of Anubis (See Below for specifics): this specialized mechanical suit that Chigaru has constructed and paid for through various legal and illegal activities. The Garb is actually an armor plated, mobile computer that covers the majority of his body. With the technological goodies he has purchased from both worlds, it has become the hacker’s wet dream given form. The armor can absorb only a few shots but protection was only a minor concern. The computer is always being updated with new hardware and software. No computer system can last long under its assault
Vehicles:
~ Self ~
Personality: Diligent when it comes to hacking but tends to be rather care free in nature.
History: History: There isn't much to say about Chigaru Bomani. Born into a well to do Rakshasain family, he never wanted for anything. Though there was a cost to the blessing of wealth, his parents were never around. To pass the time, Chiggy turned towards the computer and the internet. In time, the young man’s knowledge of computers, how they work and how to build one then as time went on, it became his only passion.
Using the sizeable ‘allowance’ that he received from his parents, Chiggy was always buying the newest and strongest upgrades that he could get his hands upon. His introduction into becoming a hacker stemmed from the computer games he used to play online. To put it frankly, he sucked at them until he was struck the idea of trying to change the game itself. Searching through hundreds of websites, he learned how to tweak the games to give him an advantage.
During his searching, he stumbled upon a website for wannabe hackers. The site enticed him and he gave it shot. Starting off small, he worked on using a modified palm to getting free drinks form soda machines. As the months went by and his skills increased, he started withdrawing money from atms and putting the funds on a cashcard. The excitement of hacking was addictive and while he stole money at times, it wasn’t because he needed the funds but due to the challenge of not getting caught.
Years passed by and Chiggy soon began hitting up entire companies, swapping funds or just wrecking playful havoc on their computer systems. Unfortunately, this time he was sloppy and wound up being arrested. Sentenced to five years in jail, it was at this time in his life that he was approached by other conflicts. Having heard of his case and disbelief at what he had done, Chiggy showed them his skills by doing minor hacking from within the prison.
Upon his release, the contacts he made set him up with a few ‘runners’. Runners are the true black op mercenaries for global companies. They take on missions ranging from escort and theft, to full scale terrorism and murder. The reason being a runner is so appealing is that they get paid obscene amounts of cash and tend to have access to government grade materials. Making contact with these runners, Chiggy’s new life began.
A few runs later, he had augmented his own body with state of the art cyberware, computer components that can be integrated with the human body. Now, his body sports a direct link between his gunsights to his eyes, data jacks to insert programs or extra memory straight into his brain but also his Deck. Deck is was he refers to his armored super computer that he wears. Its power is nearly unmatched and has the capability for him to mentally enter the cyberworld to speed up his hacking. He is now a Decker for hire, if the pay is good or job interesting enough, he’ll take it for the thrill of the hack.
Despite his prior Criminal record, Chiggy relied on the connections he made through the companies who hired him and his own family influence to land a stable programming job at the main technological hub of Rakshasa, where he get the privilege of moderating and programming the ever growing computer world.
While he may have all his needs met with that job, it still doesn’t sate his hunger for illegal high risk hacking jobs. Because of his type-A personality, he enters into the shadowlands and takes follows the command of the leading gang boss when she comes up with interesting job opportunities for him.
Garb of Anubis components
Helmet Components:
Commlink: Commlinks are the universal Matrix access device, used by everyone to be online all-the time, control all of their electronics, access their ID and accounts, and enhance their experiences with augmented and virtual reality.
Flare Compensation: This protects the user from blinding flashes of light as well as simple glare. Flare compensation also protects users with thermographic vision from heat flashes and glare from infrared lighting. It eliminates the vision modifiers for glare.
Low-Light Vision: This accessory allows the user to see normally in light levels as low as starlight. Total darkness still renders the user as blind as an unmodified person.
Micro-Transceiver: This classic short-range communication device is perfect for discreet operations. The micro- transceiver consists of an earbud and adhesive subvocal microphone (see p. 318). The transceiver’s Signal rating is equal to its Device rating.
Sensors:
Camera: The most common sensor, cameras can capture still photos, video, or trideo (including sound). Cameras may also be upgraded with vision enhancements (see p. 323).
Cyberware Scanner: This millimeter-wave scanner is primarily intended to detect cyber-implants, but can be used to identify other contraband as well. Maximum range 15 meters. See p. 255.
Directional Microphone: Allows the user to listen in on distant conversations. Solid objects as well as loud sounds outside the line of eavesdropping block the reception. Maximum range is 100 meters.
Hand and Arm components
Both hands
AR Gloves: AR Gloves: Available in all sizes and shapes, these gloves allow the user to manually interact with the Matrix, by manipulating virtual arrows, accessing a virtual keyboard or display, or remotely controlling a device. They are also equipped with force feedback, allowing for a limited tactile augmented reality experience. These gloves are also able to provide basic information regarding touched or held items, such as weight, temperature, and hardness.
Right hand
Skinlink: With skinlink, a device is adapted to send and receive data transmitted through the electrical field on the surface of metahuman skin. Though limited to touch, skinlink communication has the advantage of being protected from signal interception or jamming.
Maglock Passkey: The passkey can be inserted into a cardreader’s maglock, fooling it into believing that a legitimate passkey has been inserted.
Left Hand
Laser Microphone: This sensor bounces a laser beam against a solid object like a windowpane, reads the vibrational variations of the surface, and translates them into the sounds that are occurring on the other side of the surface.
Autopicker: This lockpick gun is a quick and effective way of bypassing mechanical locks. The autopicker’s rating added as a dice pool modifier to the Locksmith + Agility Test to pick the lock (see p. 125), or used in place of Locksmith skill if the character lacks it.
Torso and Back Components
Chameleon Suit: A full body suit made from ruthenium polymers supported by a sensor suite that scans the surroundings and replicates the images at the proper perspectives, providing the wearer with chameleon abilities. Apply a –4 dice pool modifier to Perception Tests to see the wearer. Also armored for additional protection. (This serves as the base upon which the other features have been added onto.
Software and Data Chips
Mapsoft: Mapsoft programs feature detailed information on a particular area, from streets to business/residential listings to topographical, census, GPS, and environmental data. An interactive interface allows you to quickly determine the best routes/directions, locate the nearest spot of your choice, or create your own customized maps. The mapsoft automatically updates itself with the latest data and will retrieve correlating online data (GridGuide traffic reports, restaurant menus, etc.) as necessary.
Means of connection
Fiberoptic Cable: This cable is used to establish a wired connection between two devices.
Laser Link This device allows an attached node to communicate with other laser-equipped nodes (see Beam Links, p. 51). Laser links require line of sight, and may be hampered by smoke or fog (reduce Signal by the Visibility modifier). Laser links are immune to radio-frequency jamming. (The laser link on p. 58, Arsenal, is
simply a Rating 2 laser link.)
Satellite Link: This allows the user to uplink to communication satellites in low-Earth orbit, connecting to the Matrix from places where no local wireless networks exist. This link has a Signal rating of 8. Includes a portable satellite dish.
Programs
Attack programs, anti-virus, firewalls, decryption programs, encryption programs, Key generators, password crackers, key loggers, tracking software, fake ID tags.
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= to the right in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
It’s the time of the year when darkness clocks-in sooner. Vulnerability approaches the tongue before you know it, with regret in the morning. Secrets don’t seem so bad, cause the light is gone momentarily illuminating the other side of the world. Busy late night phone lines, with foolish half-broken souls falling asleep listening to each other’s steady breathing on the other side. Did that straddle you?
Gypsy Underground is the collective name of various belly dance groups in the Anchorage area. They perform at the annual Forest Fair in Girdwood, Alaska, about 30 miles south of Anchorage. This show is one of the highlights of the Fair. This year the show was incredible with lovely graceful dancers, colorful and dazzling outfits, and even good weather for a change.
I've always loved shooting belly dancers and working with these ladies proves that life is good!
I took this photo over the 4th of July weekend, 2011.
ArtRage on iPad. The model was not short and squat, but tall and lithe; I failed in the body proportions. However, I think I caught a little of her skin's luminance.
Being a slim guy Sebastian's focus on building up his tone, and having some fun with the camera as we work to capture his routine.
All images Copyright Sim Vans. See more of my work at www.simvans.com
shot for Vortex: Fri www.vrtxmag.com/media/photo/wand-chastity-belt-the-ghost-... and Sat www.vrtxmag.com/media/photo/twin-peaks-tacocat-public-eye...
Soil profile: A representative soil profile of Trevino stony loam. Trevino soils generally are near areas of Rock outcrop and on more recent pahoehoe flows, where loess and mixed alluvial deposits are less than 50 centimeters thick to bedrock. (Soil Survey of Craters of the Moon National Monument and Preserve, Idaho; by Francis R. Kukachka, Natural Resources Conservation Service)
Landscape: Trevino soils are on basalt plains, buttes, terraces, and terrace side slopes and plug domes, lava flow lobes, pressure ridges and tumuli on shield volcanoes and lava plains. Elevations are 2,000 to 5,400 feet. The soils formed in loess and weathered volcanic ash mixed with alluvium and colluvium from basalt. Slopes are 0 to 30 percent. These soils are used mainly for rangeland and wildlife habitat.
The Trevino series consists of very shallow and shallow, well drained soils on plains. They formed in loess, alluvium, and material weathered from basalt. Permeability is moderate. Slopes are 0 to 30 percent. The average annual precipitation is about 9 inches and the average annual temperature is about 49 degrees F.
TAXONOMIC CLASS: Loamy, mixed, superactive, mesic Lithic Xeric Haplocambids
Average annual soil temperature - 47 to 56 degrees F.
Depth to bedrock - 8 to 20 inches
Depth to calcium carbonate - 8 to 18 inches
Particle-size control section
Clay content - 10 to 18 percent
Sand content - more than 15 percent coarser than VFS
Rock fragments - 0 to 35 percent including gravel, cobbles and stones
USE AND VEGETATION: Used mostly for rangeland and wildlife habitat. Some minor areas are irrigated and used for small grains, corn, beans, hay, and pasture. Potential vegetation in the natural plant community is Wyoming big sagebrush, Thurber needlegrass, and bluebunch wheatgrass.
DISTRIBUTION AND EXTENT: Southern Idaho; MLRA 11. The series is extensive.
For additional information about the survey area, visit:
www.nrcs.usda.gov/Internet/FSE_MANUSCRIPTS/idaho/cratersN...
For a detailed soil description, visit:
soilseries.sc.egov.usda.gov/OSD_Docs/T/TREVINO.html
For acreage and geographic distribution, visit:
“Some of my kin look just like trees now, and need something great to rouse them; and they speak only in whispers. But some of my trees are limb-lithe, and many can talk to me.”
― J.R.R. Tolkien
Conglomerate (lithic conglomerate) from the Cretaceous of Arkansas, USA. (8.0 centimeters across at its widest)
Sedimentary rocks form by the solidification of loose sediments. Loose sediments become hard rocks by the processes of deposition, burial, compaction, dewatering, and cementation.
There are three categories of sedimentary rocks:
1) Siliciclastic sedimentary rocks form by the solidification of sediments produced by weathering & erosion of any previously existing rocks.
2) Biogenic sedimentary rocks form by the solidification of sediments that were once-living organisms (plants, animals, micro-organisms).
3) Chemical sedimentary rocks form by the solidification of sediments formed by inorganic chemical reactions. Most sedimentary rocks have a clastic texture, but some are crystalline.
Conglomerate is a siliciclastic sedimentary rock consisting of a mix of large & small grains - it is poorly sorted. The larger grains (pebbles or cobbles or boulders) in conglomerates are rounded to subrounded in shape. The finer-grained matrix is usually sand or mud. Most conglomerates were deposited in stream/river environments or alluvial fan environments or some very shallow marine environments.
Seen here is a lithic conglomerate that is dominated by subrounded to subangular lithic pebbles and sand. This is from a lithified gravel unit that caps a famous Cretaceous-aged diamondiferous lamproite diatreme in Arkansas - the Prairie Creek Lamproite.
Stratigraphy: Tokio Formation, Upper Cretaceous, ~85 Ma
Locality: Crater of Diamonds State Park, southern Pike County, southwestern Arkansas, USA
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= to the right in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
A representative soil profile of the Crosscan series. (Soil Survey of Arches National Park, Utah; by Catherine E. Scott, Natural Resources Conservation Service)
Landscape: A typical landscape of Crosscan family-Rock outcrop complex, 5 to 30 percent slopes.
The Crosscan series consists of shallow and very shallow, well drained soils that formed in colluvium and residuum derived from sandstone and shale. Crosscan soils are in canyons and on hills. Slopes range from 6 to 80 percent. Mean annual precipitation is about 12 inches and the mean annual temperature is about 48 degrees F.
TAXONOMIC CLASS: Loamy-skeletal, mixed, superactive, calcareous, mesic, shallow Ustic Torriorthents
Note: Crosscan soils in this survey area include Lithic Ustic Torriorthents.
Soil moisture regime: aridic bordering on ustic
Soil temperature regime: mesic
Mean annual soil temperature: 52 to 54 degrees F
Depth to paralithic contact: 6 to 20 inches
Reaction: slightly or moderately alkaline
Particle-size control section: 27 to 35 percent clay
USE AND VEGETATION: These soils are used principally for wildlife habitat and livestock grazing. Dominant vegetation in the potential plant community are pinyon, juniper, mountain mahogany, and Indian ricegrass.
DISTRIBUTION AND EXTENT: Southwest Colorado. LRR D, MLRA 36. The series is of moderate extent.
For additional information about the survey area, visit:
www.nrcs.usda.gov/Internet/FSE_MANUSCRIPTS/utah/archesUT2...
For a detailed soil description, visit:
soilseries.sc.egov.usda.gov/OSD_Docs/C/CROSSCAN.html
For acreage and geographic distribution, visit:
Scientific Name: Lontra canadensis c
Description : A Characteristic of amphibious mammals is the thick and lustrous pelage. The underfur is short, dense and soft, intermixed with long guard hairs which are a glossy dark brown, usually paler on the underparts. The long vibrissae (tactile hairs) and the throat hairs are a silvery grey. The winter pelage is essentially the same as that of the summer. Well adapted to life in the water, the otter's body is long and streamlined from the bulbous nose pads to the long, tapered tail. The body is lithe and elongate as well as being solid and muscular. The comparatively small head is broad and distinctly flattened. The ears are small and may be closed underwater. The eyes are also small and somewhat anteriorly placed. The neck is scarcely narrower than the head and very muscular. The tail is also very thick and muscular and is about one-third the total length of the otter. It has short, powerful legs, the feet being large and broad with fully webbed toes. The claws are short. In adult otters, the male averages about 1% larger than the female in basic measurements and sometimes in mated pairs, the male may appear to be nearly one-third larger than a younger mate. The tail of the juvenile is relatively shorter than that of the adult, but the general appearance except for the size is similar.
Total length of adult: 90.0 to 120 cm
Tail: 30 to 47.5 cm.
Weight: 6.8 to 9 kg.
Distribution : Throughout North America, north of Mexico, except the treeless Arctic tundra and the desert areas of Texas, New Mexico, Nevada, Utah and California.
Habitat : The otter is amphibious and prefers to spend its life chiefly along rivers, larger creeks and lakes.
Food : It has a varied diet, but feeds almost exclusively on animal matter, chiefly aquatic. Minnows, sunfish, trout, catfish, sculpins and perch, and other fish are caught by direct pursuit and taken to dry land to consume. Frogs, mud puppies, crayfish, and clams are also eaten, as well as water beetles, water bugs, caddis flies, and other insects. Rarely, a muskrat, young beaver or duck may be taken.
Reproduction and Development : The North American Otter is monoestrous (reproductive cycle occurs only once a year) with a long (42 to 46 days) oestrous period during which, successive periods of heat occur about six days apart if fertilization does not take place. Delayed implantation also occurs in this species. The mating season is from late winter to early spring, immediately after the birth of the young (post-partum oestrus). The apparent gestation period varies between 9.5 and 12.5 months, including the delayed implantation period. The litter consists of two to four cubs, sometimes only one, rarely five or six. There are four mammae, all inguinal (near the groin). A newborn otter measures about 20 to 25 cm and weighs 132 g. The head is large, the tail stubby and tapered. It is furred and the eyes are closed. Growth is altricial (requiring long parental care). The eyes open after approximately 35 days and the young otters begin to play at five to six weeks of age. They venture out of their nest at 10 to 12 weeks and the female begins to teach them to swim and hunt. The male usually joins the family group after they are six months old having been driven off by the female when the young are very small. The family then stays together for about a year, the male assisting in the raising. At one year of age, the otter is nearly full grown and at two years of age, is sexually mature.
The males are not usually successful breeders until they are six to seven years old and are pugnacious only during the breeding season. Copulation usually takes place while in the water, either above or below the surface.
Adaptations : Locomotion - otters swim with swift, undulating, serpentine motion both on the surface and underwater. They swim and dive with ease, agility and speed. Progression is made chiefly with the body and tail, with only some paddling of the hind feet. A spiral motion is also used to great effect. Maximum speed on the surface is 10-12 kph and the underwater speed is almost as fast. It can stay submerged for two minutes or more, and regularly swims for considerable distances under ice, obtaining oxygen from air bubbles under the ice or open holes in the ice. They may tread water and extend the neck high above the water and peer about. Otters swim with scarcely a ripple and dive with little splashing. On land they run with the typical musteline loping gait. On soil surfaces they may run at speeds of 13-16 kph but on snow and ice where they can slide, otters may progress at a speed of 25 kph. They will take three or four leaps, then slide four to seven metres with their forelegs laid back against their sides. They travel a great deal, often covering 80 to 160 km. of stream bank during a year. Even from an established den, an otter may travel 32 to 49 km returning after an absence of several days. The home range of a mother tending her young is much less so.
Denning - the den of an otter is well-hidden and most apt to be located in a bank along a stream or lake. At times an abandoned beaver lodge is utilized. The den may be simple with short tunnels or very extensive and complicated. They may construct beds of dry wood chips, leaves and bark in hollow logs, stumps and roots. On occasion they will take over the bank burrow of a beaver or muskrat. When traveling they may make a temporary nest of grass near the water.
Senses - the only loud notes of the otter are a snarling growl when it is angry and a shrill whistle when in pain or during mating time. It also may hiss when angry, have a low purring grunt and bird-like musical chirp, evidently a call note. Its senses of smell and touch are acute. The ears may be closed underwater. The vibrissae are used when foraging along the bottom of rivers and streams.
Activity - the otter may be active any time of the day or night and although generally considered nocturnal, is more crepuscular and is often diurnal in its habits. It does not hibernate, being active year round. It is tolerant of most weather conditions. River otters are the "playful" mammals of North America. As far as anyone can tell, they appear to simply enjoy the fun of a social outing whether it be tobogganing, somersaulting underwater, playing with a rock, shooting the rapids or an earnest game of tag. An otter slide is made by the animal sliding down a slope, forming as if it were a furrowed trail in the particular spot. These slides can be quite short or several metres long. In soil they may be 15 to18 metres in length.
Threats to Survival : Hunted for their fur. Pollution of rivers and streams produces loss of habitat. Other than humans, the otter has few serious enemies. Possibly a bobcat, coyote, great horned owl or bald eagle may attempt to catch an otter kit, but the young are carefully guarded by the mother. An otter caught migrating overland is vulnerable to attack by coyotes or wolves.
Status : IUCN: Least Concern; CITES: Not Listed
Zoo Diet : Smelt, herring, TZ plain carnivore meat diet, neck bone, Thiamine tablet, Vitamin E, Dungeness crab, frozen enrichment popsicle, apples, celery, hard-boiled eggs, earthworms, crayfish, and carrots.
Toronto Zoo Website
A soil profile and landscape of a Haplogypsid from the United Arab Emirates.
Leptic Haplogypsids, sandy, mixed, hyperthermic, lithic phase (Soil AD113) are moderately to very deep, sandy soils with gypsum occurring at or near the soil surface and underlain by a lithic contact between 50cm and 200cm. They are well drained or somewhat excessively drained and permeability is moderate or moderately rapid. These soils commonly occur on older sediments in deflation plains and at the higher margins of inland and coastal sabkha. They are formed in old sand and gravel deposits.
For more information about soil classification in the UAE, visit:
library.wur.nl/isric/fulltext/isricu_i34214_001.pdf
Commonly used for low intensity camel grazing these soils frequently have less than 5% vegetation cover comprising Haloxylon salicornicum and Zygophyllum spp.
These soils are of limited extent and have been recorded in deflation plains in the north-east of the Emirate and also on the alluvial fans in the west, near Sila. The soils are a major component of one map unit and a minor component of two others.
Plate 11: Typical soil profile and associated landscape for Leptic Haplogypsids, sandy, mixed, hyperthermic, lithic phase (Soil AD113).
For additional information about the survey area, visit:
Karina Bradley wore plenty of ultra sexy outfits during the “Dance Floor Diva” Music Video shoot. But the tight red leather catsuit might have just taken things to whole new heights of exotic! It accentuated every curve in her lithe body, and it looked extra sexy on the dance floor. And for that extra touchthe diva let down her flowing blond hair.
Pop star Karina Bradley has a strong background in modeling. She even appeared in a Victoria’s Secret Fashion show. Combine that with her dance moves and glowing personality, and she has a strong musical background that flows in the club. And it came out in full force during the music video shoot. Especially when she hit the floor in her leather outfit!
Hanna Bay Member of the upper Rice Bay Formation at Graham's Harbour. This is the youngest bedrock unit on San Salvador Island.
These well-sorted limestones consist of sand-sized grains of aragonite (CaCO3). On the continents, many quartz sandstones are technically called quartz arenites. Because the sand grains making up these Bahamian rocks are calcareous (composed of calcium carbonate), the limestones are called calcarenites. When examined microscopically, the calcareous sand grains can be seen touching each other - the rock is grain-supported. This results in an alternative name for these Bahamian limestones - grainstones. “Calcarenite” seems to be a more useful, more thoroughly descriptive term for these particular rocks, so I use that, versus “grainstone” (although “calcarenitic grainstone” could be used as well). The little-used petrologic term aragonitite could also be applied to these aragonitic limestones.
Sedimentary structures indicate that the calcarenites shown above were deposited in an ancient back-beach sand dune environment. In such settings, sediments are moved and deposited by winds. Wind-deposited sedimentary rocks are often referred to as eolianites. Most ancient sand dune deposits in the rock record are composed of quartzose and/or lithic sand. The dune deposits in the Bahamas are composed of calcium carbonate - this results in the term "calcarenitic eolianite".
Hanna Bay Member limestones gently dip toward the modern ocean (= behind the photographer in the above photo) and include sediments deposited in beach environments and back-beach dune environments. The latter facies is represented by the locality shown above. Beach facies limestones are more or less planar-bedded, while back-beach dune limestones (eolianites) have steeper and more varied dips.
The aragonite sand grains in the Hanna Bay Member are principally bioclasts (worn mollusc shell fragments & coral skeleton fragments & calcareous algae fragments, etc.) and peloids (tiny, pellet-shaped masses composed of micrite/very fine-grained carbonate - some are likely microcoprolites, others are of uncertain origin).
Age: Holocene (MIS 1)
Locality: shoreline outcrop along the eastern part of the southern margin of Graham's Harbour, between Singer Bar Point and the Bahamas Field Station, northeastern San Salvador Island, eastern Bahamas
---------------------------------------
The surface bedrock geology of San Salvador consists entirely of Pleistocene and Holocene limestones. Thick and relatively unforgiving vegetation covers most of the island’s interior (apart from inland lakes). Because of this, the most easily-accessible rock outcrops are along the island’s shorelines.
------------------------------
Stratigraphic Succession in the Bahamas:
Rice Bay Formation (Holocene, <10 ka), subdivided into two members (Hanna Bay Member over North Point Member)
--------------------
Grotto Beach Formation (lower Upper Pleistocene, 119-131 ka), subdivided into two members (Cockburn Town Member over French Bay Member)
--------------------
Owl's Hole Formation (Middle Pleistocene, ~215-220 ka & ~327-333 ka & ~398-410 ka & older)
------------------------------
San Salvador’s surface bedrock can be divided into two broad lithologic categories:
1) LIMESTONES
2) PALEOSOLS
The limestones were deposited during sea level highstands (actually, only during the highest of the highstands). During such highstands (for example, right now), the San Salvador carbonate platform is partly flooded by ocean water. At such times, the “carbonate factory” is on, and abundant carbonate sediment grains are generated by shallow-water organisms living on the platform. The abundance of carbonate sediment means there will be abundant carbonate sedimentary rock formed after burial and cementation (diagenesis). These sea level highstands correspond with the climatically warm interglacials during the Pleistocene Ice Age.
Based on geochronologic dating on various Bahamas islands, and based on a modern understanding of the history of Pleistocene-Holocene global sea level changes, surficial limestones in the Bahamas are known to have been deposited at the following times (expressed in terms of marine isotope stages, “MIS” - these are the glacial-interglacial climatic cycles determined from δ18O analysis):
1) MIS 1 - the Holocene, <10 k.y. This is the current sea level highstand.
2) MIS 5e - during the Sangamonian Interglacial, in the early Late Pleistocene, from 119 to 131 k.y. (sea level peaked at ~125 k.y.)
3) MIS 7 - ~215 to 220 k.y. - late Middle Pleistocene
4) MIS 9 - ~327-333 k.y. - late Middle Pleistocene
5) MIS 11 - ~398-410 k.y. - late Middle Pleistocene
Bahamian limestones deposited during MIS 1 are called the Rice Bay Formation. Limestones deposited during MIS 5e are called the Grotto Beach Formation. Limestones deposited during MIS 7, 9, 11, and perhaps as old as MIS 13 and 15, are called the Owl’s Hole Formation. These stratigraphic units were first established on San Salvador Island (the type sections are there), but geologic work elsewhere has shown that the same stratigraphic succession also applies to the rest of the Bahamas.
During times of lowstands (= times of climatically cold glacial intervals of the Pleistocene Ice Age), weathering and pedogenesis results in the development of soils. With burial and diagenesis, these soils become paleosols. The most common paleosol type in the Bahamas is calcrete (a.k.a. caliche; a.k.a. terra rosa). Calcrete horizons cap all Pleistocene-aged stratigraphic units in the Bahamas, except where erosion has removed them. Calcretes separate all major stratigraphic units. Sometimes, calcrete-looking horizons are encountered in the field that are not true paleosols.
----------------------------
Subsurface Stratigraphy of San Salvador Island:
The island’s stratigraphy below the Owl’s Hole Formation was revealed by a core drilled down ~168 meters (~550-feet) below the surface (for details, see Supko, 1977). The well site was at 3 meters above sea level near Graham’s Harbour beach, between Line Hole Settlement and Singer Bar Point (northern margin of San Salvador Island). The first 37 meters were limestones. Below that, dolostones dominate, alternating with some mixed dolostone-limestone intervals. Reddish-brown calcretes separate major units. Supko (1977) infers that the lowest rocks in the core are Upper Miocene to Lower Pliocene, based on known Bahamas Platform subsidence rates.
In light of the successful island-to-island correlations of Middle Pleistocene, Upper Pleistocene, and Holocene units throughout the Bahamas (see the Bahamas geologic literature), it seems reasonable to conclude that San Salvador’s subsurface dolostones may correlate well with sub-Pleistocene dolostone units exposed in the far-southeastern portions of the Bahamas Platform.
Recent field work on Mayaguana Island has resulted in the identification of Miocene, Pliocene, and Lower Pleistocene surface outcrops (see: www2.newark.ohio-state.edu/facultystaff/personal/jstjohn/...). On Mayaguana, the worked-out stratigraphy is:
- Rice Bay Formation (Holocene)
- Grotto Beach Formation (Upper Pleistocene)
- Owl’s Hole Formation (Middle Pleistocene)
- Misery Point Formation (Lower Pleistocene)
- Timber Bay Formation (Pliocene)
- Little Bay Formation (Upper Miocene)
- Mayaguana Formation (Lower Miocene)
The Timber Bay Fm. and Little Bay Fm. are completely dolomitized. The Mayaguana Fm. is ~5% dolomitized. The Misery Point Fm. is nondolomitized, but the original aragonite mineralogy is absent.
----------------------------
The stratigraphic information presented here is synthesized from the Bahamian geologic literature.
----------------------------
Supko, P.R. 1977. Subsurface dolomites, San Salvador, Bahamas. Journal of Sedimentary Petrology 47: 1063-1077.
Bowman, P.A. & J.W. Teeter. 1982. The distribution of living and fossil Foraminifera and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador, Bahamas. San Salvador Field Station Occasional Papers 1982(2). 21 pp.
Sanger, D.B. & J.W. Teeter. 1982. The distribution of living and fossil Ostracoda and their use in the interpretation of the post-Pleistocene history of Little Lake, San Salvador Island, Bahamas. San Salvador Field Station Occasional Papers 1982(1). 26 pp.
Gerace, D.T., R.W. Adams, J.E. Mylroie, R. Titus, E.E. Hinman, H.A. Curran & J.L. Carew. 1983. Field Guide to the Geology of San Salvador (Third Edition). 172 pp.
Curran, H.A. 1984. Ichnology of Pleistocene carbonates on San Salvador, Bahamas. Journal of Paleontology 58: 312-321.
Anderson, C.B. & M.R. Boardman. 1987. Sedimentary gradients in a high-energy carbonate lagoon, Snow Bay, San Salvador, Bahamas. CCFL Bahamian Field Station Occasional Paper 1987(2). (31) pp.
1988. Bahamas Project. pp. 21-48 in First Keck Research Symposium in Geology (Abstracts Volume), Beloit College, Beloit, Wisconsin, 14-17 April 1988.
1989. Proceedings of the Fourth Symposium on the Geology of the Bahamas, June 17-22, 1988. 381 pp.
1989. Pleistocene and Holocene carbonate systems, Bahamas. pp. 18-51 in Second Keck Research Symposium in Geology (Abstracts Volume), Colorado College, Colorado Springs, Colorado, 14-16 April 1989.
Curran, H.A., J.L. Carew, J.E. Mylroie, B. White, R.J. Bain & J.W. Teeter. 1989. Pleistocene and Holocene carbonate environments on San Salvador Island, Bahamas. 28th International Geological Congress Field Trip Guidebook T175. 46 pp.
1990. The 5th Symposium on the Geology of the Bahamas, June 15-19, 1990, Abstracts and Programs. 29 pp.
1991. Proceedings of the Fifth Symposium on the Geology of the Bahamas. 247 pp.
1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Abstracts and Program. 26 pp.
1992. Proceedings of the 4th Symposium on the Natural History of the Bahamas, June 7-11, 1991. 123 pp.
Boardman, M.R., C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The geology of Columbus' landfall: a field guide to the Holcoene geology of San Salvador, Bahamas, Field trip 3 for the annual meeting of the Geological Society of America, Cincinnati, Ohio, October 26-29, 1992. Ohio Division of Geological Survey Miscellaneous Report 2. 49 pp.
Carew, J.L., J.E. Mylroie, N.E. Sealey, M. Boardman, C. Carney, B. White, H.A. Curran & D.T. Gerace. 1992. The 6th Symposium on the Geology of the Bahamas, June 11-15, 1992, Field Trip Guidebook. 56 pp.
1993. Proceedings of the 6th Symposium on the Geology of the Bahamas, June 11-15, 1992. 222 pp.
Lawson, B.M. 1993. Shelling San Sal, an Illustrated Guide to Common Shells of San Salvador Island, Bahamas. San Salvador, Bahamas. Bahamian Field Station. 63 pp.
1994. The 7th Symposium on the Geology of the Bahamas, June 16-20, 1994, Abstracts and Program. 26 pp.
1994. Proceedings of the 5th Symposium on the Natural History of the Bahamas, June 11-14, 1993. 107 pp.
Carew, J.L. & J.E. Mylroie. 1994. Geology and Karst of San Salvador Island, Bahamas: a Field Trip Guidebook. 32 pp.
Godfrey, P.J., R.L. Davis, R.R. Smtih & J.A. Wells. 1994. Natural History of Northeastern San Salvador Island: a "New World" Where the New World Began, Bahamian Field Station Trail Guide. 28 pp.
Hinman, G. 1994. A Teacher's Guide to the Depositional Environments on San Salvador Island, Bahamas. 64 pp.
Mylroie, J.E. & J.L. Carew. 1994. A Field Trip Guide Book of Lighthouse Cave, San Salvador Island, Bahamas. 10 pp.
1995. Proceedings of the Seventh Symposium on the Geology of the Bahamas, June 16-20, 1994. 134 pp.
1995. Terrestrial and shallow marine geology of the Bahamas and Bermuda. Geological Society of America Special Paper 300.
1996. The 8th Symposium on the Geology of the Bahamas, May 30-June 3, 1996, Abstracts and Program. 21 pp.
1996. Proceedings of the 6th Symposium on the Natural History of the Bahamas, June 9-13, 1995. 165 pp.
1997. Proceedings of the 8th Symposium on the Geology of the Bahamas and Other Carbonate Regions, May 30-June 3, 1996. 213 pp.
Curran, H.A., B. White & M.A. Wilson. 1997. Guide to Bahamian Ichnology: Pleistocene, Holocene, and Modern Environments. San Salvador, Bahamas. Bahamian Field Station. 61 pp.
1998. The 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-June 8, 1998, Abstracts and Program. 25 pp.
Wilson, M.A., H.A. Curran & B. White. 1998. Paleontological evidence of a brief global sea-level event during the last interglacial. Lethaia 31: 241-250.
1999. Proceedings of the 9th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 4-8, 1998. 142 pp.
2000. The 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2000, Abstracts and Program. 29+(1) pp.
2001. Proceedings of the 10th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2000. 200 pp.
Bishop, D. & B.J. Greenstein. 2001. The effects of Hurricane Floyd on the fidelity of coral life and death assemblages in San Salvador, Bahamas: does a hurricane leave a signature in the fossil record? Geological Society of America Abstracts with Programs 33(4): 51.
Gamble, V.C., S.J. Carpenter & L.A. Gonzalez. 2001. Using carbon and oxygen isotopic values from acroporid corals to interpret temperature fluctuations around an unconformable surface on San Salvador Island, Bahamas. Geological Society of America Abstracts with Programs 33(4): 52.
Gardiner, L. 2001. Stability of Late Pleistocene reef mollusks from San Salvador Island, Bahamas. Palaios 16: 372-386.
Ogarek, S.A., C.K. Carney & M.R. Boardman. 2001. Paleoenvironmental analysis of the Holocene sediments of Pigeon Creek, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 17.
Schmidt, D.A., C.K. Carney & M.R. Boardman. 2001. Pleistocene reef facies diagenesis within two shallowing-upward sequences at Cockburntown, San Salvador, Bahamas. Geological Society of America Abstracts with Programs 33(4): 42.
2002. The 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6th-June 10, 2002, Abstracts and Program. 29 pp.
2004. The 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-June 7, 2004, Abstracts and Program. 33 pp.
2004. Proceedings of the 11th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 6-10, 2002. 240 pp.
Martin, A.J. 2006. Trace Fossils of San Salvador. 80 pp.
2006. Proceedings of the 12th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 3-7, 2004. 249 pp.
2006. The 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-June 12, 2006, Abstracts and Program. 27 pp.
Mylroie, J.E. & J.L. Carew. 2008. Field Guide to the Geology and Karst Geomorphology of San Salvador Island. 88 pp.
2008. Proceedings of the 13th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 8-12, 2006. 223 pp.
2008. The 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-June 16, 2006, Abstracts and Program. 26 pp.
2010. Proceedings of the 14th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 12-16, 2008. 249 pp.
2010. The 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-June 21, 2010, Abstracts and Program. 36 pp.
2012. Proceedings of the 15th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 17-21, 2010. 183 pp.
2012. The 16th Symposium on the Geology of the Bahamas and Other Carbonate Regions, June 14-June 18, 2012, Abstracts with Program. 45 pp.
There are a number of "Galaxy"stones on this site with the apparent "Great Divide" line; the immense ridge running similar in theory to a longitude line. In geology a mountain ridge with sequential subduction layers becomes exaggerated when the earth's crust moves and shifts placing pressure on the neighboring less movable sections of our Earth's Crust, thus creating the Earth's crust to buckle gradually rising into a mountain ridge. The fact that this "Great Divide" line comes up repeatedly on the stones from this site indicates that this ridge is a huge issue for those in our galaxy capable of celestial travel; perhaps this entire ridge became more pronounced 3 Billion Years ago when the Dwarf Galaxy collided with the primary core of our galaxy. The upper and lower left quadrants of this stone perhaps show definitive evidence of how the collision took place3 Billion years ago separating huge portions of the celestial core of our primary galaxy that was shifted and now lies more below than above this "Great Divide" geographic anomaly. It was 65 Million years ago that a devastating asteroid hit the Yucatan Peninsula roughly 10 Kilometers in circumference; so if our Milky Way Galaxy collided with a smaller dwarf galaxy roughly 3 Billion years ago, whatever celestial geographic mechanism ; this celestial part of our galaxy in Section l was virtually upended and the entire Section I region of our galaxy was basically thrown in utter chaos and reorganized with the constant bombardment of celestial events that our modern world could most likely not even imagine or experience within a single life time.
If you study the surface of this stone; the green celestial symbol in the upper left quadrant is only a small element of the actual green pigment on the surface of this stone; however the narrative of that single multi-faceted totemic symbol with three linear pairs of symbols and the third, the highest pair of symbols, appears to reveal an outstretched arm with perhaps a small figural image of man facing left-ward towards a celestial sphere then following celestial triangulation marker leading to three linear symbols on the upper-left edge of the stone, with the green markers descending below the figure along the left edge of this stone is a series of green symbols descending along the left edge of this stone ultimately reaching the lower left quadrant where there is a definitive pyramid structural overlay opening to the opposite side of the stone; perhaps aligned with the concept of a celestial portal marker, as found on many other stones from this site???
If you return back to the previous floral photo and study the detail of the floral mechanism on a macro scale; then return to identify the multitude of small green micro symbols across the surface of this stone this process will help train your eye to see and understand the micro detail that this ancient culture world's existed in; it will slowly become easier to study the micro detail on the surfaces of stones from this site.
The region around the triangular opening on this stone in the lower left quadrant appears to be peppered with cloud-like accumulations of sone kind of culture and then mixed with green pigment micro markings, perhaps these two different white and green entities mark at least two different (green:small and white:large) core civilizations on Earth???
The elongated green symbol in the upper left quadrant appears to transition to a white figure on the interior and opposite side of the "Great Divide line"; leading to Section II and III.
There are virtually two basic rounded mountain peaks on the upper edge of this "Galaxy Stone" with the darker recessed bowl symbol representing a celestial being with a bird's beak and this symbol descending along the far right to a smaller ochre hourglass-like figure making up the forehead and twin-peaked crowned headdress of right facing image of man on the far right edge of this stone.
The interior side of the ochre symbol in the upper right quadrant is marked with an approximate 120 degree outer edge angle pointing towards a pair of twin celestial green astrolabe markers, most likely necessary for successful celestial navigation we still do not understand.
The entire golden ochre region on the right side of the "Great Divide" line is peppered with blackened diagrams on the ochre and small micro (barely visible) green markers spread across this ochre region like a thin blanket descending to the lower middle hypotenuse line/edge of this stone, Earth's location. I can identify a variety of micro green symbols on the right side of the "Great Divide" descending to the lower edge where Earth's position would be sitting within the middle of this lower hypotenuse galaxy edge-line.
The multitude of micro green markers embedded within the golden ochre pigment on the right side of the "Great Divide Line perhaps help fulfill a celestial narrative of how celestial life could possibly exist on our side of the Milky Way galaxy.
Each stone on this site is like book onto itself and studying the individual green markers on the surface of this stone is an extended micro journey onto itself; North America, culture unknown.
Notice the pale dark-blue light echo in the upper left quadrant.
Time will tell.
Photo Copyright 2012, dynamo.photography.
All rights reserved, no use without license
+++++ FROM WIKIPEDIA ++++
Hong Kong (Chinese: 香港; pronunciation in Hong Kong Cantonese: [hœ́ːŋ.kɔ̌ːŋ]), officially the Hong Kong Special Administrative Region of the People's Republic of China, is an autonomous territory on the eastern side of the Pearl River estuary in East Asia, south of the mainland Chinese province of Guangdong, and east of the former Portuguese colony and fellow special administrative region of Macau. With around 7.3 million Hong Kongers of various nationalities[note 1] in a territory of 1,104 km2, Hong Kong is the fourth-most densely populated region in the world.
Hong Kong was formerly a colony of the British Empire, after the perpetual cession of Hong Kong Island from Qing China at the conclusion of the First Opium War in 1842. The colony expanded to the Kowloon Peninsula in 1860, and acquired a 99-year lease of the New Territories from 1898. Hong Kong was later occupied by Japan during the Second World War, until British control resumed in 1945. The territory was returned to China under the framework of the Sino-British Joint Declaration, signed between the United Kingdom and China in 1984 and marked by the transfer of sovereignty of Hong Kong in 1997, when it became a special administrative region of the People's Republic of China.[13]
Under the principle of "one country, two systems",[14][15] Hong Kong maintains a separate political and economic system apart from China. Except in military defence and foreign affairs, Hong Kong retains independent executive, legislative, and judiciary powers.[16] Nevertheless, Hong Kong does directly develop relations with foreign states and international organizations in a broad range of "appropriate fields",[17] being actively and independently involved in institutions such as the Asia-Pacific Economic Cooperation forum[18] and the World Trade Organization.[19]
Hong Kong is one of the world's most significant financial centres, holding the highest Financial Development Index score and consistently ranking as the world's most competitive and freest economic entity.[20][21] As the world's eighth-largest trading entity,[22] its legal tender, Hong Kong dollar, is the world's 13th most traded currency.[23] Hong Kong's tertiary sector dominated economy is characterised by competitive simple taxation and supported by its independent judiciary system.[24] Although the city boasts one of the highest per capita incomes in the world, it suffers from severe income inequality.[25]
Hong Kong features the most skyscrapers in the world, surrounding Victoria Harbour, which lies in the centre of the city's dense urban region.[26][27] It has a very high Human Development Index ranking and the world's longest life expectancy.[28][29] Over 90% of its population makes use of well-developed public transportation.[30] Seasonal air pollution with origins from neighbouring industrial areas of mainland China, which adopts loose emissions standards, has resulted in a high level of atmospheric particulates in winter.[31][32][33]
Etymology
Hong Kong
Hong Kong in Chinese 2.svg
"Hong Kong" in Chinese characters
Chinese 香港
Cantonese Yale Hēunggóng or Hèunggóng
Literal meaning Fragrant Harbour,
Incense Harbour[34][35]
[show]Transcriptions
Hong Kong Special Administrative Region
Traditional Chinese 香港特別行政區
(香港特區)
Simplified Chinese 香港特别行政区
(香港特区)
Cantonese Yale Hēunggóng Dahkbiht Hàhngjingkēui
(Hēunggóng Dahkkēui)
or
Hèunggóng Dahkbiht Hàhngjingkēui
(Hèunggóng Dahkkēui)
[show]Transcriptions
The name Hong Kong originally referred to a small inlet between Aberdeen Island and the southern coast of Hong Kong Island. The town of Aberdeen was an initial point of contact between British sailors and local fishermen.[36] The source of the romanised name is not known, but it is generally believed to be an early imprecise phonetic rendering of the spoken Cantonese pronunciation of 香港 (Cantonese Yale: hēung góng), which means "Fragrant Harbour" or "Incense Harbour".[34][35][37] Fragrance may refer to the sweet taste of the harbour's fresh water influx from the Pearl River estuary or to the incense from factories lining the coast of northern Kowloon. The incense was stored near Aberdeen Harbour for export before Victoria Harbour was developed.[37] Another theory is that the name originates from the Tanka, early inhabitants of the region; it is equally probable that a romanisation of the name in their dialect was used (i.e. hōng, not hēung in Cantonese).[38] Regardless of origin, the name was recorded in the Treaty of Nanking to encompass all of Hong Kong Island, and has been used to refer to the territory in its entirety ever since.[39]
The name had often been written as the single word Hongkong until the government adopted the current form in 1926.[40] Nevertheless, a number of institutions founded during the early colonial era still retain the single-word form, such as the Hongkong Post, Hongkong Electric, and the Hongkong and Shanghai Banking Corporation.
History
Archaeological studies support human presence in the Chek Lap Kok area from 35,000 to 39,000 years ago and on Sai Kung Peninsula from 6,000 years ago.[41][42][43] Wong Tei Tung and Three Fathoms Cove are the earliest sites of human habitation in Hong Kong during the Paleolithic Period. It is believed that the Three Fathom Cove was a river-valley settlement and Wong Tei Tung was a lithic manufacturing site. Excavated Neolithic artefacts suggested cultural differences from the Longshan culture of northern China and settlement by the Che people, prior to the migration of the Baiyue to Hong Kong.[44][45] Eight petroglyphs dated to the Shang Dynasty were discovered on the surrounding islands.[46]
Imperial China
Main article: History of Hong Kong under Imperial China
In 214 BC, the Qin dynasty conquered the Baiyue tribes in Jiaozhi (modern-day Liangguang region and Vietnam) and incorporated the area of Hong Kong into China for the first time.[47] After a brief period of centralisation and subsequent collapse of the Qin dynasty, the area of Hong Kong was consolidated under the Nanyue kingdom, founded by general Zhao Tuo in 204 BC.[48] After the Han conquered Nanyue in 111 BC, Hong Kong was assigned to the Jiaozhi commandery. Archaeological evidence indicates an increase of population and expansion of salt production. The Lei Cheng Uk Han Tomb on the Kowloon Peninsula is believed to have been built as a burial site during the Han dynasty.[49]
Sung Wong Toi, believed to be a memorial to the last two boy emperors of the Southern Song dynasty, as it appeared before the Second Sino-Japanese War.
During the Tang dynasty, the Guangdong region flourished as an international trading center. A military stronghold was established in Tuen Mun to strengthen defence of the coastal area.[50] Lantau Island was a salt production centre and smuggler riots occasionally broke out against the government. The first village school, Li Ying College, was established around 1075 in the modern-day New Territories by the Song dynasty.[51] During their war against the Mongols, the Southern Song court was briefly stationed at modern-day Kowloon City (the Sung Wong Toi site) before their ultimate defeat at the Battle of Yamen in 1279.[52]
The earliest European visitor on record was Jorge Álvares, a Portuguese explorer, who arrived in 1513.[53][54] Having established a trading post in a site they called "Tamão" in Hong Kong waters, Portuguese merchants commenced with regular trading in southern China. Subsequent military clashes between China and Portugal, however, led to the expulsion of all Portuguese merchants from southern China.[55] After the Qing conquest, Hong Kong was directly affected by the Great Clearance, an imperial decree that ordered the evacuation of coastal areas of Guangdong from 1661 to 1669 as part of his efforts against Ming loyalist rebels in southern China. Over 16,000 inhabitants of Xin'an County, which included Hong Kong, were forced to migrate inland; only 1,648 of those who had evacuated returned in subsequent years.[56] With frequent pirate attacks and ever increasing incursions by European explorers, forts were constructed at Tung Chung and the Kowloon Walled City.[57]
Though maritime trade had previously been banned, after repopulation of the coast and final defeat of all rebels with Ming sympathies, the Kangxi Emperor lifted the trade prohibition in 1684 and allowed foreigners to enter Chinese ports.[58] Trade with Europeans was more strictly regulated and became concentrated in the Pearl River Delta after establishment of the Canton System in 1757, which forbade non-Russian ships from northern Chinese ports and forced all commerce to be conducted solely in the port of Canton, just north of Hong Kong.[59] While European demand for Chinese commodities like tea, silk, and porcelain was high, Chinese interest in European manufactured goods was comparatively negligible, creating a large trade imbalance between Qing China and Great Britain. To counter this deficit, the British began to sell increasingly large volumes of Indian opium to China.[60] Faced with a drug addiction crisis,[61] Chinese officials pursued ever more aggressive actions in an attempt to halt the opium trade.[60]
British colony
In 1839, threats by the Qing imperial court to place sanctions on opium imports caused diplomatic friction with the British Empire. Tensions escalated into the First Opium War. After British victory in the Second Battle of Chuenpi, the Qing initially admitted defeat. As part of a ceasefire agreement between Captain Charles Elliot and Qishan, Viceroy of Liangguang, Hong Kong Island was declared to be ceded under the Convention of Chuenpi. British forces took formal possession of the island on 26 January 1841. However, disputes between high-ranking officials of both countries led to the failure of the treaty's ratification.[62] After more than another year of further hostilities, Hong Kong Island was formally ceded in perpetuity to the United Kingdom under the terms of the Treaty of Nanking on 29 August 1842.[63] The British officially established a Crown colony and founded the City of Victoria in the following year.[64]
The population of Hong Kong Island was 7,450 when the Union Jack raised over Possession Point on 26 January 1841. It mostly consisted of Tanka fishermen and Hakka charcoal burners, whose settlements scattered along several coastal hamlets. In the 1850s, a large number of Chinese refugees crossed the open border fleeing from the Taiping Rebellion. Other natural disasters, such as flooding, typhoons, and famine in mainland China would play a role in establishing Hong Kong as a place for safe shelter.[65][66] Further conflicts over the opium trade between the British and Qing quickly escalated into the Second Opium War. Following the Anglo-French victory, the colony was expanded to include Kowloon Peninsula (south of Boundary Street) and Stonecutter's Island, both of which were ceded to the British in perpetuity under the Convention of Beijing in 1860. The colony was expanded further in 1898, when Britain obtained a 99-year lease of additional territory from the Qing under the Convention for the Extension of Hong Kong Territory; Lantau Island, the area north of Boundary Street in Kowloon up to the Sham Chun River, and over 200 other outlying islands were given over to British control.[67][68][69]
Queen's Road Central at the junction of Duddell Street, c. 1900
Hong Kong soon became a major entrepôt thanks to its free port status, attracting new immigrants from both China and Europe. However, the population remained racially divided and polarised under early British colonial policies. Despite the rise of a British-educated Chinese upper-class by the late-19th century, racial discrimination laws, such as the Peak Reservation Ordinance, prevented ethnic Chinese from acquiring property in reserved areas, such as Victoria Peak. At this time, the majority of the Chinese population in Hong Kong had no political representation in the British colonial government. The British governors did rely, however, on a small number of Chinese elites, including Sir Kai Ho and Robert Hotung, who served as ambassadors and mediators between the government and local population.
The colony continued to experience modest growth during the first half of the 20th century. The University of Hong Kong was established in 1911 as the territory's first higher education institute. While there had been an exodus of 60,000 residents for fear of a German attack on the British colony during the First World War, Hong Kong remained unscathed. Its population increased from 530,000 in 1916 to 725,000 in 1925 and reached 1.6 million by 1941.[70]
In 1925, Cecil Clementi became the 17th Governor of Hong Kong. Fluent in Cantonese and without a need for translators, Clementi appointed Shouson Chow to the Executive Council as its first ethnic Chinese member. Under Clementi's tenure, Kai Tak Airport entered operation as RAF Kai Tak and several aviation clubs. At the outbreak of the Second Sino-Japanese War in 1937, when the Empire of Japan invaded China from its protectorate in Manchuria, Governor Geoffry Northcote declared the colony a neutral zone to safeguard Hong Kong's status as a free port.
Japanese military occupation
On 8 December 1941, the same morning as the attack on Pearl Harbor, the Imperial Japanese Army moved south from Guangzhou and crossed the Sham Chun River to attack Hong Kong as part of a coordinated military offensive against the Allied Powers.[71] The Battle of Hong Kong lasted for 17 days, through which British, Canadian, Indian, and local colonial units defended Hong Kong. By the fifth day, Commonwealth troops, under heavy artillery and aerial bombardment, had been forced to abandon their positions in Kowloon and retreated to Hong Kong Island.[72] With the remaining troops unable to further mount an effective defence, Governor Young surrendered the colony on Christmas Day. This day is remembered by locals as "Black Christmas".[73]
During the occupation, the garrisoned Japanese soldiers committed many atrocities against both civilians and prisoners of war, including the St. Stephen's College massacre. Local residents suffered widespread food shortages, strict rationing, and hyperinflation arising from the forced exchange of currency from Hong Kong dollars to Japanese military yen. Widespread starvation and forced deportation of residents for use as slave labour to mainland China drastically reduced the population of Hong Kong from 1.6 million in 1941 to 600,000 in 1945, when control of the colony returned to the British.[74]
Post-war industrialisation
Hong Kong's population recovered quickly after the war, as a wave of skilled migrants from the Republic of China sought refuge from the Chinese Civil War in a territory neutral to the conflict. When the Communist Party took full control of mainland China in 1949, even more refugees fled across the open border in fear of persecution.[67] Many newcomers, especially those who had been based in the major port cities of Shanghai and Guangzhou, established corporations and small- to medium-sized businesses and shifted their base operations to British Hong Kong.[67] The establishment of the People's Republic of China caused the British colonial government to reconsider Hong Kong's open border to mainland China. In 1951, a boundary zone was demarked as a buffer zone against potential military attacks from communist China. Border posts along the north of Hong Kong began operation in 1953 to regulate the movement of people and goods into and out of the territory.
In the 1950s, Hong Kong became the first of the Four Asian Tiger economies that was undergoing rapid industrialisation driven by textile exports, manufacturing industries, and re-exports of goods to China. As the population grew, with labour costs remaining low, living standards began to rise steadily.[75] The construction of the Shek Kip Mei Estate in 1953 marked the beginning of the public housing estate programme, which provided shelter for the less privileged and helped cope with the continuing influx of immigrants.
Under Governor Murray MacLehose, the government began a series of reforms to improve the quality of infrastructure and public services through the 1970s. Systemic corruption in the uniformed services had crippled trust in the government; MacLehose established the ICAC, an independent security service under the direct authority of the Governor, to restore the integrity of the civil service.[76] Chinese was recognised as an official language during his tenure, accelerating the process of localisation in the government, slowly handing key official posts long held only by British members of the government over to local ethnic Chinese people.[77][78] To alleviate road traffic congestion and provide a more reliable means of crossing the Victoria Harbour, the Mass Transit Railway was constructed and began operations of its first line in 1979. The Island Line, Kwun Tong Line, and Tsuen Wan Line all opened in the early 1980s, connecting Hong Kong Island, Kowloon, and parts of the New Territories to a single transport system.[79] MacLehose was the longest-serving colonial governor and, by the end of his governorship, had become one of the most popular and well-known figures in the territory. MacLehose laid the foundation for Hong Kong to establish itself as a key global city in the 1980s and early 1990s.
Since 1983, the value of the Hong Kong dollar has been pegged to that of the United States dollar. The territory's competitiveness in manufacturing gradually declined due to rising labour and property costs, as well as new industrial capacity developed in southern China under the Open Door Policy, which was introduced in 1978. Nevertheless, by the early 1990s, Hong Kong had established itself as a global financial centre, a regional hub for logistics and freight, one of the fastest-growing economies in Asia, and the world's exemplar of laissez-faire market policy.[80]
The Hong Kong issue
In 1971, China's permanent seat on the United Nations Security Council was transferred from the Republic of China, which had evacuated to Taiwan at the conclusion of the Chinese Civil War, to the People's Republic of China. Hong Kong was soon after removed from the organization's list of non-self-governing territories, at the request of the PRC. Facing an uncertain future for the colony and the expiration of the New Territories lease beyond 1997, Governor MacLehose raised the question of Hong Kong's status with Deng Xiaoping in 1979.
Diplomatic negotiations with China resulted in the Sino-British Joint Declaration in 1984. The United Kingdom agreed to transfer to China the entirety of the colony, including the perpetually ceded areas of Hong Kong Island and Kowloon Peninsula, at the conclusion of the 99-year New Territories lease in 1997, when Hong Kong would become a special administrative region governed separately from the mainland, retaining its free-market economy, common law judicial system, independent representation in international organizations, treaty arrangements, and self-governance in all areas except foreign diplomacy and military defence. The treaty further stipulated that the territory would be guaranteed a high degree of autonomy for at least 50 years after the transfer, with the Basic Law of Hong Kong serving as its constitutional document.[67]
Under the terms of the Second Convention of Peking, the colony was expanded out to the New Territories, but the treaty did not include a small military outpost over which the Kowloon Walled City would later be built. After the end of Japanese occupation, thousands of refugees fleeing from the mainland during the Chinese Civil War made their way to the Walled City and became squatters occupying this parcel of land where China was technically still the sovereign power. Over the following decades, the population of this 2.6-hectare (6.4-acre) area dramatically increased, reaching 33,000 by 1987, making the Walled City the most densely populated area in the world at its peak.[81][82] Despite widespread illegal activity and unsanitary living conditions, the British largely took a 'hands-off' approach with regard to the Walled City due to the area's muddled territorial status and to avoid confrontation with the mainland authority.[83] The Sino-British Joint Declaration laid the groundwork for cooperation between the British and Chinese governments concerning any Hong Kong-related issues, including the fate of the former military fort. The Chinese government acquiesced to the demolition of the settlement in 1987.[84] The structure was cleared away in 1994 and the area converted into the Kowloon Walled City Park.[85]
Transfer of sovereignty
On 1 July 1997, sovereignty over Hong Kong was officially transferred from the United Kingdom to the People's Republic of China, marking the end of 156 years of British colonial rule. As Britain's last major and most populous remaining colony, the handover effectively represented the end of the British Empire. This event made Hong Kong the first special administrative region of China. Exactly at midnight, all government organisations with royal patronage simultaneously dropped the Royal prefix from their titles and any regalia with references to the Crown were replaced with insignia bearing the Bauhinia.[86] After the handover ceremony, Chris Patten, the last Governor of Hong Kong, together with Prince Charles, departed the city on board the Royal Yacht Britannia.[87]
Special administrative region
Almost immediately after the transfer of sovereignty, Hong Kong's economy was severely affected by the Asian financial crisis and further depressed by the outbreak of the H5N1 strain of avian flu. Financial Secretary Donald Tsang used the substantial territorial foreign currency reserves to maintain the Hong Kong dollar's currency peg and spent over HK$120 billion on significant holdings of major Hong Kong companies to prevent a general market collapse.[67] While complete disaster was averted, Chief Executive Tung's housing policy of building 85,000 subsidised flats a year triggered a housing market crisis in 1998, depressing property prices and causing some homeowners to become bankrupt.[88] Hong Kong was again gravely affected by the outbreak of severe acute respiratory syndrome (SARS) in 2003.[89][90] In total, 1,755 people were infected, with 299 fatalities.[91] Economic activities slowed and schools were closed for weeks at the height of the epidemic. An estimated HK$380 million (US$48.9 million) in contracts were lost as a result of the epidemic.[92] While Hong Kong was also severely affected by the global recession of the late 2000s, the Tsang government introduced a series of economic stimulus measures prevented a prolonged recession.[93]
Infrastructure post-handover has been rapidly developed, with major transport links continuing to be planned and constructed. The Rose Garden Project, which began under British administration, to construct a new international airport was completed in 1998 and operations began at the new site during the same year. The Ngong Ping Cable Car, West Kowloon Cultural District, multiple new railway lines, and additional cross-harbour tunnels were all completed in the first 20 years of territorial self-governance. Direct infrastructure links with mainland China are also being actively developed, with both the Hong Kong–Zhuhai–Macau Bridge and Hong Kong section of the national high-speed railway currently under construction. Construction of the rail link generated a high level of controversy surrounding the demolition of key landmarks and displacement of residents along the planned route.[94]
Hong Kong Island north coast, overlooking Victoria Harbour and Central and East Kowloon from middle section of Lugard Road at daytime
Political debates have centred themselves predominately on issues surrounding electoral reform and Hong Kong's jurisdictional independence from the central government. Following the handover, democratic reform of the Legislative Council was immediately terminated and the government attempted to legislate sweeping national security legislation pursuant to Article 23 of the Basic Law. Coupled with years of economic hardships and discontent of Chief Executive Tung's pro-Beijing stance, over 500,000 people demonstrated against the government, which eventually led to Tung's resignation in 2005.[95] Further proposals by the government to introduce a national education curriculum and nominee pre-screening before allowing Chief Executive elections triggered a number of mass protests in 2014, collectively known as the Umbrella Revolution.[96] Violent attacks on journalists, an increasing level of press self-censorship, alleged extraterritorial abduction of anti-China publishers,[97] and covert intervention into Hong Kong's educational, political, and independent institutions have posed challenges to the policy of one country, two systems. In the 2016 legislative election, there were reports of discrepancies in the electorate registry, which contained ghost registrations across constituencies, as well as political intervention to strip pro-independence individuals of their right to stand in elections[98] and alleged death threats to election candidates.[99] Social tension heightened during Leung's term, with many residents believing that China increased their efforts to exert influence on everyday life in Hong Kong. A survey in 2016 showed that only 17.8% of residents considered themselves as "Chinese citizens", whereas 41.9% considered themselves purely as "citizens of Hong Kong".[100]
Government and politics
香港候任特首林鄭月娥13.jpg 政務司司長張建宗15.jpg
Hong Kong is a special administrative region of China, maintaining a separate legislature, executive, and judiciary from the rest of the country. It has a parliamentary government modelled after the Westminster system, inheriting this from British colonial administration. The Sino-British Joint Declaration guarantees the territory's capitalist economic system and autonomous system of government for 50 years after the transfer of sovereignty.[note 2] Under this framework, the Basic Law of Hong Kong is the regional constitutional document, establishing the structure and responsibility of the government.[101][102] The head of government is the Chief Executive, who is selected by the Election Committee for a five-year term that is renewable once. The central government provides oversight for the regional government; final interpretative power of the Basic Law rests with the Standing Committee of the National People's Congress and the Chief Executive is formally appointed by the State Council after nomination by the aforementioned Election Committee.[101] Responsibility for foreign and military affairs is also assumed by the central authority.[note 3]
Government House, official residence of the Chief Executive.
A chamber within the Legislative Council Complex.
The grey dome and front gable of a granite neo-classical building, with a skyscraper in the background against a clear blue sky.
Court of Final Appeal Building in Central. Formerly housed the Supreme Court and the Legislative Council before its current function.
The Legislative Council is a unicameral legislature with 70 members, consisting of 35 directly elected members apportioned to geographical constituencies, 30 members representing professional or special interest groups formed as functional constituencies, and 5 members nominated by members of the District Councils and elected in territory-wide elections.[14][103] Legislators are elected using multiple different voting systems, determined by whichever constituency a particular seat is representing. All directly elected seats are filled using a proportional representative system, while functional constituencies other than the all-territory District Council constituency choose their councillors using first-past-the-post or instant-runoff voting.[104]
Government policy is determined by the Executive Council, a body of advisors appointed by the Chief Executive with the authority to issue delegated legislation and proposes new bills to the legislature for debate and promulgation. Direct administration is managed by the Civil Service, an apolitical bureaucracy that ensures positive implementation of policy.[14][105] Hong Kong is nationally represented in the National People's Congress by 36 delegates chosen through an electoral college.[16][106]
22 political parties had representatives elected to the Legislative Council in the 2016 election.[107] These parties have aligned themselves into three ideological groups: the pro-Beijing camp who form the current government, the pro-democracy camp, and localist groups.[108] The Communist Party does not have an official political presence in Hong Kong and its members do not run in local elections.[109]
The judicial system of Hong Kong is derived from the common law system of English law, and was created at the establishment of the territory as a British colony. Chinese national law does not generally apply in the region, and Hong Kong is treated as an independent jurisdiction.[112] The Court of Final Appeal is the territory's highest court, exercising final adjudication over interpretation of laws and has the power to strike down statutes and legislation inconsistent with the Basic Law.[113][114] It is led by the Chief Justice and consists of three additional permanent judges and one non-permanent seat filled by judges from overseas common law jurisdictions on a rotating basis.[14][115] However, final interpretation of the Basic Law itself is a power vested in the Standing Committee of the National People's Congress. Judges on all courts are appointed by the Chief Executive on the recommendation of an independent commission.[14][116] As a common law system, judicial courts in Hong Kong may refer to precedents set in English law and Commonwealth jurisdictions.[14][115][14]
The Department of Justice is responsible for handling legal matters for the government. Its responsibilities include providing legal advice, criminal prosecution, civil representation, legal and policy drafting and reform and international legal co-operation between different jurisdictions.[112] Apart from prosecuting criminal cases, lawyers of the Department of Justice act on behalf of the government in all civil and administrative lawsuits against the government.[112] The department may call for judicial review of government action or legislation and may intervene in any cases involving the greater public interest.[117] The Basic Law protects the Department of Justice from any interference by the government when exercising its control over criminal prosecution.[14][118] Law enforcement is a responsibility of the Security Bureau and the Hong Kong Police, with agencies like the Customs and Excise Department and Immigration Department handling more specialised tasks.
Foreign relations
Though no longer administering the territory after the transfer of sovereignty, the United Kingdom maintains strong ties with Hong Kong. Hundreds of British corporations maintain offices or their regional headquarters in the territory,[123] and both parties collaborate on a number of economic and bilateral agreements.[124][125] Hong Kong regularly invites British and Commonwealth judges to sit on the Court of Final Appeal,[126] and its universities remain involved in the Association of Commonwealth Universities.[127] As a party to the Sino-British Joint Declaration, the United Kingdom is obligated to ensure proper implementation of the treaty; the Foreign Secretary gives biannual reports to Parliament on the status of Hong Kong.[128]
Regional and administrative divisions
Hong Kong consists of three geographical regions, divided by their time of acquisition by the United Kingdom: Hong Kong Island, Kowloon, and the New Territories. The city of Victoria, the first urban settlement in Hong Kong, was established on Hong Kong Island, and its area is analogous to present-day Central and Western District.
The territory is administratively divided into 18 districts. Each district is represented by a district council, which advises the government on local issues such as the provisioning of public facilities, maintenance of community programmes, promotion of cultural activities, and improvement of environmental policies.[131] There are a total of 541 district council seats, 412 of which are directly elected and 27 of which are filled by ex officio members consisting of rural committee chairmen, representing villages and towns of outlying areas of the New Territories; the remaining seats are appointed by the Chief Executive.[131] The Home Affairs Department communicates government policies and plans to the public through the district offices.[132] Local administration of municipal services was previously delegated to the Urban Council in Kowloon and Hong Kong Island and to the Regional Council in the New Territories, until they were abolished in 1999.
The main territory of Hong Kong consists of a peninsula bordered to the north by Guangdong province, an island to the south east of the peninsula, and a smaller island to the south. These areas are surrounded by numerous much smaller islands.
Electoral and political reforms
Main article: Democratic development in Hong Kong
Although the Basic Law lays the foundation for the regional government, some of its articles require more specific legislation to be adopted before implementation. Article 23 provides for laws that prohibit treason and subversion in the territory, and a bill was drafted pursuant to this constitutional requirement. The government dropped this proposal after fierce opposition and protests against its perceived potential to restrict freedom of information.[16][133]
Articles 45 and 68 state that the ultimate goal is for both the Chief Executive and all members of the Legislative Council to be selected by universal suffrage.[17] While the legislature is now partially directly elected, the executive continues to be selected by means other than direct election. From its establishment as a colony, Hong Kong has not had a fully representative democratic government. Colonial administration prior to the Second World War largely excluded Chinese representation.[134] As a British territory, the executive was embodied by the Sovereign, who appointed and was personally represented by the Governor. The Legislative Council initially consisted exclusively of appointed white British members, with its first Chinese member not joining the chamber until 1880.[135] After the end of Japanese occupation and the resumption of British control, amidst the greater movement of global decolonisation, the government seriously considered constitutional reform in Hong Kong; this was ultimately shelved due to fears of government infiltration by communist sympathisers after their victory at the conclusion of the Chinese Civil War.[136]
Presentation of an electoral reform consultation report in 2014
Electoral reform continues to be a contentious issue after the transfer of sovereignty. The government faces ongoing calls to introduce direct election of the Chief Executive and all Legislative Council members.[141] These efforts have been partially successful; the Election Committee no longer selects a portion of the Legislative Council and was slightly expanded to 1,200 members, and the number of legislature seats was increased to 70.[142] A central government decision in 2014 to require Chief Executive candidates to be pre-screened as part of a reform package to introduce universal suffrage incited large-scale protests demanding a more open process.[143] The proposal was later rejected by the legislature and the executive selection process remains unchanged.
Sociopolitical issues and human rights
The Standing Committee of the National People's Congress holds final interpretative power over the Basic Law, and use of it can override any regional judicial process. After the 2016 legislative elections, six incoming Legislative Council members took their oaths of office improperly. The Standing Committee subsequently issued a new interpretation of the Basic Law article regarding assumption of office, preempting a territorial judicial review and allowing the High Court to disqualify the legislators.[148][149] Judicial independence was also questioned after the disappearance of five staff members of a Causeway Bay bookstore that was known to sell literary material prohibited in the mainland.[150] Their possible abduction and rendition by Chinese public security bureau officials would represent a breach of the Sino-British Joint Declaration, violating the guarantee of regional autonomy;[151] mainland authorities do not have extraterritorial jurisdiction to enforce national laws.[144]
Freedom of the press since the handover have been threatened by incidents of physical violence against journalists and as news media organisations are pressured not to publish stories that portray the central government in a negative way.[152][153] News media has been increasingly prone to self-censorship, as publication owners expand business interests on the mainland or media organisations become acquired by Chinese corporations.[154][155] The police have been accused of using excessive force against protesters at public rallies and overtly barring demonstrators from free assembly.[156][157]
Ethnic minorities, excluding those of European ancestry, have marginal representation in government and are often discriminated against while seeking housing, education, and employment opportunities.[158][159] While legislation prohibits discrimination based on age, sex, and disability, it specifically excludes migrant workers, along with immigrants and mainland Chinese.[160][161] Employment vacancies and public service appointments frequently have language requirements, which minority job seekers frequently fail to meet, while language education resources remain inadequate for Chinese learners.[162][163] In recent years, residents of a minority ethnicity have been more frequently placed on government advisory committees to address racial issues.[164]
Under current law, Chinese citizens resident in Hong Kong are unable to enlist in the armed forces and are not subject to conscription as prescribed in the Chinese constitution.[172] The People's Liberation Army sponsored the establishment of the Hong Kong Army Cadets Association, a uniformed youth organization of children aged 6 and older.[173]
Geography
Topographical satellite image with enhanced colours showing areas of vegetation and conurbation. Purple areas around the coasts indicate the areas of urban development
Areas of urban development and vegetation are visible in this false-colour satellite image
Hong Kong is located on China's south coast, 60 km (37 mi) east of Macau on the opposite side of the Pearl River Delta. It is surrounded by the South China Sea on the east, south, and west, and borders the Guangdong city of Shenzhen to the north over the Sham Chun River. The territory's 2,755 km2 (1,064 sq mi) area consists of Hong Kong Island, the Kowloon Peninsula, the New Territories, and over 200 offshore islands, of which the largest is Lantau Island. Of the total area, 1,106 km2 (427 sq mi) is land and 1,649 km2 (637 sq mi) is water. Hong Kong claims territorial waters to a distance of 3 nautical miles (5.6 km). Its land area makes Hong Kong the 167th largest inhabited territory in the world.[174]
Higher-altitude areas of Hong Kong are often dominated by grassland: Lantau Island during the dry season
This will be the last of the Fall series … I hope. I don’t think I have suffered so much pain and humiliation for “Art” … even boot camp in the summer sun in Texas was more fun! Ever peel 500 pounds of potatoes with a hand peeler? And, that was just for breakfast!
Anyway, here it is. This small tree, about 25 feet tall, was sandwiched between larger cypress trees of little distinction. An ugly chain link fence to the right and an ugly large electrical box to the left. Hence, the portrait orientation. In the center of it all, this little beauty basking in the last rays of Autumn light. Out of the way, a wall flower. Alas, a few days later, she looked ridden hard, whipped, and put away abused and muddy. The wind, rain, snow, and overnight freeze was her demise. Her 8,267 veils have fallen from her lithe frame.
After my recent interaction with Chuck these last few days, I know her pain and loss of dignity. But, time is on our side, little tree. We will return next year bigger, better, and stronger! And, taller! And, armed! And, ….
Maybe a little better on black.
Mytilus californianus Conrad, 1837 - articulated California mussel shell (modern) on a lithic pebble beach in California, USA.
Bivalves are bilaterally symmetrical molluscs having two calcareous, asymmetrical shells (valves) - they include the clams, oysters, and scallops. In most bivalves, the two shells are mirror images of each other (the major exception is the oysters). They occur in marine, estuarine, and freshwater environments. Bivalves are also known as pelecypods and lamellibranchiates.
Bivalves are sessile, benthic organisms - they occur on or below substrates. Most of them are filter-feeders, using siphons to bring in water, filter the water for tiny particles of food, then expel the used water. The majority of bivalves are infaunal - they burrow into unlithified sediments. In hard substrate environments, some forms make borings, in which the bivalve lives. Some groups are hard substrate encrusters, usually using a mineral cement to attach to rocks, shells, or wood.
The fossil record of bivalves is Cambrian to Recent. They are especially common in the post-Paleozoic fossil record.
Seen here is the interior surface of an articulated California mussel shell, Mytilus californianus. This species occurs along the western coasts of northern Mexico, America, Canada, Alaska and into the Aleutian Islands. California mussels are sessile, benthic, epifaunal, filter-feeding, hard substrate encrusters that are abundant in many intertidal rocky shore environments. Mussels extrude an organic material called byssus, in the form of byssal threads, to attach to hard substrates (rockgrounds, hardgrounds, etc.).
Classification: Animalia, Mollusca, Bivalvia, Pteriomorphia, Mytiloida, Mytilidae
Locality: Rodeo Beach, western side of the Marin Peninsula, northwest of San Francisco, Pacific Coast of central California, USA (37° 49' 50.84" North latitude, 122° 32' 16.30" West longitude)
-------------------------
See info. at:
en.wikipedia.org/wiki/California_mussel
and
inverts.wallawalla.edu/Mollusca/Bivalvia/Mytiloida/Mytili...
Lakeshore beach gravel in the Holocene of Minnesota, USA.
This is modern beach gravel along the northern shoreline of western Lake Superior. Most of the clasts are pebble-sized (= 4 to 64 mm). The gray-colored pebbles are derived from lakeshore outcrops of basalt lava flows. The pinkish- & dark pinkish-colored pebbles are eroded from rhyolite lava flows. The original basalt and rhyolite outcrops are part of a lava flow-dominated succession called the North Shore Volcanic Group. This is equivalent to & the same age as the Portage Lake Volcanic Series of northern Michigan's Keweenaw Peninsula (www.flickr.com/photos/jsjgeology/albums/72157632266738191). The North Shore and Portage Lake successions are ~1.1 billion years old and represent basalt lava flows, plus minor sedimentary rocks, that filled up an ancient rift valley. This old rift is the Lake Superior segment of the Mid-Continent Rift System, a tear in the ancient North American paleocontinent of Laurentia (see: minerals.usgs.gov/science/midcontinent-rift-minerals/imag...). Tectonic rifting started along this tear, exactly like the modern-day East African Rift Valley. Laurentia's Mid-Continent Rift System started and then stopped and was subsequently filled and buried. This ancient failed rift is now exposed on either side of Lake Superior in North America's Great Lakes.
The pebbles were transported and deposited by waves and longshore currents.
Provenance: North Shore Volcanic Group, Keweenawan Supergroup, upper Mesoproterozoic, ~1.1 Ga
Locality: Lake Superior shoreline in Leif Ericson Park, just northeast of the city of Duluth, northeastern Minnesota, USA
Conglomerate (lithic conglomerate) from the Cretaceous of Arkansas, USA. (8.0 centimeters across at its widest)
Sedimentary rocks form by the solidification of loose sediments. Loose sediments become hard rocks by the processes of deposition, burial, compaction, dewatering, and cementation.
There are three categories of sedimentary rocks:
1) Siliciclastic sedimentary rocks form by the solidification of sediments produced by weathering & erosion of any previously existing rocks.
2) Biogenic sedimentary rocks form by the solidification of sediments that were once-living organisms (plants, animals, micro-organisms).
3) Chemical sedimentary rocks form by the solidification of sediments formed by inorganic chemical reactions. Most sedimentary rocks have a clastic texture, but some are crystalline.
Conglomerate is a siliciclastic sedimentary rock consisting of a mix of large & small grains - it is poorly sorted. The larger grains (pebbles or cobbles or boulders) in conglomerates are rounded to subrounded in shape. The finer-grained matrix is usually sand or mud. Most conglomerates were deposited in stream/river environments or alluvial fan environments or some very shallow marine environments.
Seen here is a lithic conglomerate that is dominated by subrounded to subangular lithic pebbles and sand. This is from a lithified gravel unit that caps a famous Cretaceous-aged diamondiferous lamproite diatreme in Arkansas - the Prairie Creek Lamproite.
Stratigraphy: Tokio Formation, Upper Cretaceous, ~85 Ma
Locality: Crater of Diamonds State Park, southern Pike County, southwestern Arkansas, USA
3.3 million years of lithic rock tools, then and only then, everything else!
Miner in a jacklegging contest during Mining Week, Yellowknife, Northwest Territories, Canada. This was back when both the Con and Giant gold mines were operating. Whoever buries two steels in the shortest time, wins. Best keep your fingers in your ears, jacklegging is LOUD.