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>-----Original Message----- >From: Pranoto, Imanuel W >Sent: Wednesday, February 02, 2005 4:19 PM >To: iagi-net@iagi.or.id >Subject: RE: [iagi-net-l] Re: Paleo-Tsunami > >Amin, >Mungkin link ini bisa membantu mengenai shallow marine tsunami >deposit di Teluk Banten akibat erupsi Krakatau 1883. > >http://www.nioz.nl/public/mcg/publications/van_den_bergh_2003.pdf > >Kalau server-nya saya bisa kirim lewat japri. > >------ >Salam, >Noel > >>-----Original Message----- >>From: [EMAIL PROTECTED] [mailto:[EMAIL PROTECTED] >>Sent: Wednesday, February 02, 2005 2:05 PM >>To: iagi-net@iagi.or.id >>Subject: [iagi-net-l] Re: Paleo-Tsunami >> >>Kira-kira di P . Jawa ada tidak singkapannya? >> >>============================= >>AMIR AL AMIN - DKS/OPG/WGO >>TOTAL E&P INDONESIE >>BALIKPAPAN >>(62-542)-534283 - (62)-811592277 >>============================= >> >>http://www.sthjournal.org/213/scheff.pdf >> >>CHEVRON-SHAPED ACCUMULATIONS ALONG THE COASTLINES OF AUSTRALIA AS >>POTENTIAL TSUNAMI EVIDENCES? >>Dieter Kelletat >>Anja Scheffers >>Geographical Department, University of Duisburg-Essen >Universitätsstr. >>15 >>D-45141 Essen, Germany >>e-mail: [EMAIL PROTECTED] >>ABSTRACT >>Along the Australian coastline leaf- or blade-like chevrons appear at >>many places, sometimes similar to parabolic coastal dunes, but often >>with unusual shapes including curvatures or angles to the coastline. >>They also occur at places without sandy beaches as source areas, and >>may be truncated by younger beach ridges. Their dimensions reach >>several kilometers inland and altitudes of more than 100 m. >Vegetation >>development proves an older age. Judging by the shapes of the >chevrons >>at some places, at least two generations of these forms can be >>identified. This paper discusses the distribution patterns of >chevrons >>(in particular for West Australia), their various >appearances, and the >>possible genesis of these deposits, based mostly on the >interpretations >>of aerial photographs. >>Science of Tsunami Hazards, Volume 21, Number 3, page 174 >>(2003) 1. INTRODUCTION The systematic monitoring of tsunami >during the >>last decades has shown that they are certainly not low frequency >>events: on average, about ten events have been detected every >year ? or >>more than 1000 during the last century (Fig. 1, NGDC, 2001) ? many of >>which were powerful enough to leave imprints in the >geological record. >>Focusing only on the catastrophic events, we find for the last 400 >>years (Fig. 2, NGDC, 2001) that 92 instances with run up of more than >>10 m have occurred, >>39 instances with more than 20 m, and 14 with more than 50 m, or ? >>statistically and without >>counting the Lituya Bay events ? one every 9 years with more >than 20 m >>run up worldwide. >>Considering at least 300,000 years of a high sea level during the >>Pleistocene epoch of more than >>2 Mio. years, and assuming that the frequency of strong tsunami for >>those times was about the same as during the last centuries, the >>world's coastlines have been hit by about 30,000 tsunami with run up >>heights of more than 20 m during high sea levels of the Quaternary ? >>and we know nearly nothing about their contribution to >coastal forming. >>Strikingly, so far no systematic investigation of tsunami or >>paleo-tsunami imprints exists, and nearly all of their traces >have been >>detected coincidentally. On the other hand, many attempts to prove >>historically documented mega events by finding their >geological traces >>have failed. With this background in mind and referring to >the state of >>the art of tsunami field evidences, we will discuss chevron >forms along >>the Australian coastline with regard to their suitability as >>paleo-tsunami indicators, particularly because we urgently need more >>reliable indicators for tsunami events in the landscape. This >>regional-scale study for West Australia is based on aerial photograph >>interpretation. The aim is to differentiate the entire spectrum of >>morphological types of chevrons in different coastal environments >>covering a wide range of latitudes and deduce indicators of their age >>and genesis. >>However, this remote sensing >>approach has to be completed with a detailed sediment analyses and >>absolute dating techniques. >>During the last years, several coastal forms and deposits have been >>identified that could be related to formerly unknown paleo-tsunami >>(Bryant et al., 1996; Bryant, 2001; Mastronuzzi & Sanso, >2001; Kelletat >>& Schellmann, 2002; Scheffers, 2002, and others). On the one hand, >>there are huge dislocated boulders or groups of boulders appearing as >>significant landscape marks and as evidences for extremely high >>transport energies, and on the other hand, there may be Fig. 1: >>Number of registered >>tsunami per century from >>about 2000 BC (NGDC, >>2001). >>Science of Tsunami Hazards, Volume 21, Number 3, page 175 >>(2003) smaller forms of rock sculpturing due to very strong tsunami >>currents, the latter, in particular, differentiated by Bryant (2001). >>But for even the largest dislocated coastal boulders (of more >than 1000 >>t), some authors (Talandier & Bourrouilh-Le-Jan, 1988, for the >>Tuamotu-Archipelago, or Hearty et al., 1998, for the Bahamas) >prefer to >>believe that their genesis is caused by storm impact rather than >>tsunami. >>The chevrons (large sandy coastal deposits discussed in this paper), >>however, have not been proven in detail to be of tsunamigenic origin. >>To date, they have been mentioned in only a few papers >(Bryant et al., >>1997; Bryant, 2001; Bryant & Nott, 2001, and Hearty et al., 1998, >>Kindler & Strasser, 2000), and for only two regions >(Australia and the >>Bahamas). >>Whereas the Australian examples have been described as tsunamigenic >>(from the Younger Holocene), the Bahamian features have been >related to >>catastrophic storms from the last interglacial. >>The intention of this study is to discuss whether the so-called >>chevrons may have a much wider distribution, and whether they may be >>clues for extreme tsunami impacts in a very extended area >that have not >>yet been described. >>Fig. 2: High run up values during the last 400 years (NGDC, 2001). >>Science of Tsunami Hazards, Volume 21, Number 3, page 176 >>(2003) 2. CHEVRONS: DEFINITION, CHARACTER AND AGE According to Hearty >>et al. (1998) chevrons are "v-shaped, sublinear to parabolic, >>ribbonlike? >>depositional landforms", containing "beach fenestrae" and other >>"water-made structures." >>On the Bahamas, where they can appear along 700 km of coastline, they >>are made by "many waves acting over a short time interval" or >>"organized sets of large waves." Their average size there is >3 km long >>(max. 10 km!), a third of this as width, their ridges or >ribbons may be >>20 to 100 m wide, and they have a relative height of 8 to 25 >m (max. 40 >>m) with the highest section in the distal parts. A central elongated >>depression is normally enclosed by the ridges. The chevrons >are mostly >>sandy, but may contain pebble beds and clasts, often from aeolianite >>(on the Bahamas). >>They may be accompanied by huge boulders of up to 2000 t at 11 m asl. >>and 500 m distant to the shoreline, and have been dated on the last >>interglacial oxygen-isotope substage 5e at around 123,000 ± 5000 BP. >>The depositional forces should be extreme storms developed during a >>significant climatic revolution at the end of isotope substage 5e >>(Hearty et al., 1998). The genesis of chevrons as water made >>structures, however, is still under debate. >>Kindler & Strasser (2000), who >>did not know of the 2000 t boulders accompanied with the Bahamian >>chevrons and did not find clasts in these features, interpret >the forms >>as parabolic dunes from a lower sea level of isotope substage 5e in a >>phase of a dryer climate, and interpret the beach fenestrae >in them as >>made by heavy rain. >>Bryant et al. (1997), Bryant & Nott (2001), and Bryant (2001) >described >>chevrons from SE- and W-Australia up to 30 km inland and 130 m high. >>They are often mapped as coastal dunes, because they >sometimes resemble >>parabolic aeolian accumulations, but they may contain shell, clasts, >>and well rounded cobbles. At least in one place in West >Australia, they >>have been dated to 1080 AD. >>3. CHEVRON DISTRIBUTION ALONG THE AUSTRALIAN COASTLINES According to >>Bryant (2001) and Bryant & Nott (2001), chevrons occur at >Jervis Bay in >>New South Wales and around Point Samson near Port Hedland in >the NW of >>West Australia. >>In this section we will describe and interpret the very extended >>chevron distribution along Australia's coastlines on the basis of >>selected aerial photographs and topographic maps. >>Although sediment analysis has yet not been done, the various shapes, >>their relation to other coastal forms, their evidently older >formation, >>their relation to the modern dominant wind patterns or to >ancient dune >>systems, can be discussed, and some general conclusions regarding the >>age and forming processes can be given. None of the regions mentioned >>below have ever been analyzed regarding a tsunamigenic source of the >>chevron forms and sediments. Because of the extreme extent of >>Australia's coastline, the analysis presented in this paper has a lot >>of regional gaps, of course. >>3.1 Northern Territory >>In the Roper River district near the mouth of the Rose river >(i.e., the >>western section of the Gulf of Carpentaria) along a coastal >stretch of >>at least 40 km, chevrons are developed in a low Science of Tsunami >>Hazards, Volume 21, Number 3, page 177 >>(2003) coastal landscape. Their length may exceed 3 km, their >altitude >>at least >>33 m. Their axis is 135°- >>140°, which describes the direction of the forming forces. >The chevrons >>are inactive and densely vegetated, evidently older than a >beach ridge >>system that truncates their seaward basal parts. >>3.2 Queensland (Fig. 3) >>In the Cape Melville area (about 90 km SW of the cape) south of the >>mouth of the Jeannie River, a set of chevrons has developed along at >>least 10 km of coastline, formed from the SE (about 160°). All are >>inactive and densely vegetated. They start at beaches, as >well as along >>low coastlines without sand. Clearly distinguishable are two >different >>types of >>chevrons: an older one, hard to identify on aerial photographs, of up >>to 5 km in length, broad and partly eroded, and a strip of >younger ones >>with clear contours, about 1 km inland, that are decorated by coastal >>swamps formed by the blocking of the run-off from the coastal plains. >>Fig. 3: >>Two generations of chevrons near >>the mouth of the Jeannie River, SW >>of Cape Melville, Queensland. >>3.3 Victoria >>Possible chevrons at Cape Bridgewater near Portland, extending across >>the broad tombolo of this cape, accumulated from the west, densely >>vegetated. Nearly 4 km long and up to 20 m high. >>Science of Tsunami Hazards, Volume 21, Number 3, page 178 (2003) >>3.4 West Australia (along the south coast from E to W, and along the >>west coast from S to N) >>a) Cape Arid National Park: >>Along the bays W and E of the southernmost cape in the National Park, >>chevrons have accumulated from WSW, up to 6 km inland, and 40 to 60 m >>high in the western section. Vegetated, but the sand is partly >>mobilized again by strong winds. >>b) Albany and environs (Fig. 4): >>In the east and, in particular, to the west of Albany, the bays are >>decorated by leaf-like or lanceolate deposits along more than 30 km, >>extending inland for more than >>3 km, some parts with >>heights of more than 100 m. They even appear on rocky headlands and >>along coastal sections without beaches or other sources of sandy >>material. Their general elongation is SSW to NNE, but in some places >>they start at the coastline from the south, bending to the east and >>back again to NE. This produces a flame-like form. Their >outer contours >>are sharply marked, but in places, younger sand drift masks the >>contours. The chevrons are covered by vegetation including bushes and >>small trees, pointing to an active phase longer ago (at least >>centuries). Around headlands, clear refraction patterns of >the chevrons >>can be detected. Another typical aspect in the Albany region is an >>exactly parallel inner pattern of smaller chevrons, repeated >up to five >>times within the larger form, producing an overall, swash-like shape >>(Fig. 5). >>Fig. 4: Extended chevrons near Albany with refraction patterns around >>headlands, curvatures, and well developed, even along rocky >shorelines. >>Science of Tsunami Hazards, Volume 21, Number 3, page 179 >>(2003) Fig. 5: >>Chevrons enclosed within larger forms from the Albany and >Walpole area. >>Fig. 6: >>Refraction and curvatures of chevrons, and their development, even >>along cliff shorelines near Walpole. >>Science of Tsunami Hazards, Volume 21, Number 3, page 180 >>(2003) Fig. 7: The Cape Leeuwin Peninsula is widely decorated >by large >>chevrons from the west. >>c) Irwin Inlet, about 6 km S of Walpole (Fig. 6): >>Chevrons on both sides of the inlet, from SW and WSW, up to 5 >km inland >>and up to 150 m high. Mostly along a rocky shoreline, from about >>250°-260°, vegetated, with refraction patterns around headlands. >>d) Northcliffe: >>Chevrons at least 7 km long, some >>more than 100 m high, mostly along a >>steeper coast or cliffs without beaches, vegetated, from the west >>(250°-270°). >>e) White Point E Augusta: >>This bay E of Augusta near Cape >>Leeuwin is decorated by chevrons along >>its entire length of >30 km, in the eastern part around 2 km >inland, in >>the western part up to 3 km, with heights of 30 to 40 m. Along the >>eastern part of the bay, chevrons top cliff sections, in the western >>part they start along beaches. Their long axis changes from >WSW in the >>east to S to SSE in the west, showing a clear refraction pattern that >>does not correspond to the main wind directions. Despite some active >>blowouts, the chevrons are inactive forms again. >>f) Cape Leeuwin area (Fig. 7): >>The rocky western coast of this cape shows chevrons extending >>4 km inland from the west. >>To the north, they bend a little toward 280°-290°. Their height is >>about 40 m to more than 100 m asl.. Some of the chevrons >widen to their >>distal parts, giving the shape of oak leaves. Characteristic are gaps >>in the chevron formation, which are not orientated to headlands or >>rocky shores. >>g) Bunbury: >>Smaller chevrons along sandy beaches, but inactive and covered by >>vegetation, reaching about 1 km inland and mostly 20 to 30 m high. >>Science of Tsunami Hazards, Volume 21, Number 3, page 181 (2003) >>h) Mandurah/Pinjarra: >>Shorter chevrons (about 1 km in length), extending at least >30 km along >>sandy beaches, formed from westerly directions, partly destroyed by >>younger drifting sands, vegetated, heights up to 40 m. Their coastal >>sections may be truncated by younger beach ridge sequences (Fig. 8). >>i) North of Perth (Fig. 9): >>Chevrons up to 5 km inland, from the west, along at least 60 km of >>narrow beaches, highest around 40 m, from about 250°-270°. >Older forms >>further inland are mostly destroyed, and a younger set is clearly >>marked in spite of vegetation cover. In contrast to other areas, the >>chevrons show an "oak leaf" appearance. >>j) Beagle Island N Perth: >>Steep coast with small beaches. Chevrons several kilometers >long and 30 >>m high, from 190°-200°, i.e., in a small angle to the coastline. Here >>they resemble inactive parabolic coastal dunes. >>k) Dongara S Geraldton: >>The chevrons accompany a low cliff for about 30 km directly north of >>Dongara, further north they follow a narrow beach, reaching 2 km >>inland, mostly 20 m high, max. 60 m, formed from the south >(180°-200°). >>In the southern portion, they resemble inactive parabolic dunes. >>l) Geraldton: >>North and south of the town, chevrons have been formed from southerly >>directions (180°-190°, i.e., in an angle to the coastline), >partly with >>drifting sand, up to 40 m high and less than 2 km long. >>m) Edel, Tamala and Denham: >>West of Shark Bay, chevrons decorate the outer peninsulas, crossing >>them for several kilometers, but are never developed on peninsulas >>protected from the open ocean. Up to 80 m high, forms are >very similar >>to terrestrial elongated and parabolic dunes. Formed directly >from the >>south. >>Fig. 8: Although fine sediments are available, chevron >development was >>followed by beach ridge formation during the Younger Holocene near >>Mandurah and Pinjarra south of Perth. >>Fig. 9: Many chevrons north of Perth show an oak leaf appearance. >>Science of Tsunami Hazards, Volume 21, Number 3, page 182 (2003) >>n) Carnavon: >>North of the town, broad beach ridges with remnants of older and >>truncated chevrons behind, changing about 18 km north of the >town into >>parabolic forms directly contacting the beaches. >>Length is about 1 to 3 km, height 10 to 28 m. >>o) Quobba (Fig. 10): >>Around Red Bluff, about 40 km N of Point Quobba, chevrons from >>190°-200°, at Point Quobba more towards 180°, i.e., parallel to the >>coastline. It seems that they continue inland in a field of parabolic >>and elongated older dunes. >>Chevrons some kilometers long, on top of cliffs, some more than 100 m >>asl. >>p) Ningaloo (Fig. 11): >>Similar appearance to point Quobba: from the south (180°-210°), some >>kilometers long, changing into a parabolic dune field inland, height >>more than 20 m. Partly active blowouts and sand drift. The >chevrons may >>partly cover a system of small beach ridges. >>Fig. 10: Chevrons near Point Quobba are very similar to parabolic >>dunes. >>Fig. 11: Chevrons close to the Ningaloo reef may originate along >>beaches or cliff lines, and partly cover older Holocene beach ridge >>systems. >>4. GENERAL CONCLUSIONS FROM THE >>MORPHOLOGIC ASPECTS AND DISTRIBUTION >>AS ARGUMENTS FOR A TSUNAMIGENIC >>ORIGIN OF CHEVRONS >>Based on the distribution patterns of the chevrons, their orientation >>to the coastlines, their relation to other coastal forms (such as >>cliffs, headlands, or beach ridges), the source of loose material (in >>particular sand), geomorphic aspects, freshness of forms, and >>vegetation cover, it is possible to draw some general conclusions: >>Science of Tsunami Hazards, Volume 21, Number 3, page 183 (2003) >>a) Chevrons of one to several kilometers in length and >heights of 10 m >>to more than 120 m are distributed around the coastline of Australia >>(i.e., Gulf of Carpentaria, Cape York Peninsula, New South >Wales, south >>and west coast of West Australia), with a clear dominance in the west >>of the continent. >>b) Chevrons may be formed perpendicular to-, parallel to-, or >in angles >>to the coastline. >>c) They usually have a straight axis, but at some places they >can bend >>in two directions and change their main direction by up to >90° (Fig. 5 >>and 12). >>Fig. 11: >>Chevrons close to the Ningaloo reef may originate along beaches or >>cliff lines, and partly cover older Holocene beach ridge systems. >>d) Their outer contours are relatively sharply marked, >particularly the >>parts that are furthest inland. These parts may be the highest. >>e) Chevrons continue from the coastline to heights of more >than 120 m, >>even in a rocky environment without sandy sources. >>The forming forces have been strong enough to reach several >kilometers >>inland, as well as high up on steep slopes. >>f) Many chevron formations show simple contours (i.e., only single >>ribbons or ridges framing a central depression), but others >have up to >>five enclosed ridges that are smaller but strongly parallel (Fig. 5). >>This is due to several waves, not to several forming generations >>differing in time. >>Science of Tsunami Hazards, Volume 21, Number 3, page 184 (2003) >>g) Most chevrons are narrower to their landward side (Fig. >>12), but some widen inland, resembling oak leaves (Fig. 9). >>h) The chevrons have a swash-like appearance that differs >from that of >>coastal dunes. Typically, chevron formations can have smaller gaps >>without chevrons, and this appearance differs markedly from >coastlines >>with shifting dunes (which do not have such gaps). >>i) Along curved beaches in rounded bays, the direction of the chevron >>axis may change, corresponding to the normal wave approach in bays, >>which is always perpendicular to the beaches. >>j) On opposing sides of a headland, the chevrons may have different >>directions due to refraction. >>k) The sources for the chevron material may be beaches, but chevrons >>also occur often at locations where there is no beach, but instead, >>cliffs or steeper coastal slopes. At these locations the material can >>only derive from the foreshore environments. >>l) All chevrons are inactive forms, covered by vegetation and soil, >>even in the dry western environments. Their relation to the active >>coastline, however, proves their Holocene maximum age. >>m) In some regions, at least two generations of Holocene chevrons can >>be detected. The older, landward chevrons are much more eroded and >>often difficult to detect on aerial photographs (Fig. 3). >>n) An older Holocene age is shown by the existence of sequences of >>younger beach ridges seaward of the chevrons, which have destroyed or >>reworked the chevron's basal parts (Fig.8). At other places, chevrons >>have covered older Holocene beach ridge patterns. >>o) Areas of chevron development are sometimes not suitable >for coastal >>dunes because of the lack of sand, the presence of mangrove >fringes or >>other dense coastal vegetation (Fig. 3 and North Queensland), or >>seaward dominant wind directions. >>p) Because of their similar appearance and clearness of form, >at least >>the younger chevron generation along the south and west coast of West >>Australia seems to be from the same event at least some 100 >years ago. >>This is in contradiction to an origin as coastal dunes, because they >>developed successively over a longer time. >>q) The direction of the chevrons in some places coincides with >>predominant regional winds or the fossil dune patterns of terrestrial >>Australia (see Fig. 13), but in other places, this is not the case. >>r) All chevron patterns can be explained by one or two >extreme tsunami. >>For West Australia, >>the source of the tsunami cannot be Réunion Island with the >collapse of >>the Píton de la Fournaise volcano in 4200 BP (see Labazuy, 1996), >>because from this distance, the wave pattern should be more or less >>parallel from the west along the entire coastline. At the southern >>coast, however, waves from west to southwest with a >refraction pattern >>to southerly directions appear around Cape Leeuwin, along the central >>western coast the dominant direction is west, and in the >northern parts >>of West Australia they change to the southerly direction. This can be >>explained by a tsunami source at a nearer distance (e.g., >about 1000 km >>to reach coastlines along more than 2000 km of the continent) >near the >>latitude of Perth (see Fig. 14). >>The origin may be a large submarine slide or a meteorite. >>s) There are evidences that West Australia (and other coasts such as >>northern Queensland or New South Wales) have been affected by >extremely >>strong tsunami in the past. They have transported sand, shell, and >>cobble up to 30 km inland, and up to 60 m, or even 130 m, in height >>Science of Tsunami Hazards, Volume 21, Number 3, page 185 (2003) >>(Bryant et al., 1997; Bryant & Nott, 2001, Bryant, 2001), and have >>decorated several places along the coastline (Quobba, Cape >Leveque, New >>South Wales, etc.) with large boulder fields > 30 m asl.. >>Fig. 13: Direction of chevron axes, fossil dune patterns, and modern >>wind systems. >>5. CONCLUSIONS >>Of course, the hypothesis that chevrons are swash forms from tsunami >>must be proven in the field with more evidence than is known >today, in >>particular, by analyzing their sediments and by dating. On the other >>hand, it would be difficult to explain all of the chevrons presented >>here as coastal dunes, because to do so would require a rather >>complicated evolutionary history consisting of at least: >>Science of Tsunami Hazards, Volume 21, Number 3, page 186 (2003) >>a) A first phase of coastal dune development during the >middle Holocene >>with a sea level lower than today's to expose sand for blow out in >>foreshore regions of modern cliffs and submerging slopes, and with a >>wind pattern different from today's. >>b) A phase without coastal dune development for several >thousand years, >>but with beach ridge formation at places where sand was available. >>c) A second phase of coastal dune development, rather short, >about 1000 >>years ago, again with a lower sea level to mobilize fine >sediments from >>foreshore regions, and again with a wind pattern different from >>today's. >>d) No significant coastal dune development for the last >several hundred >>years, and the establishment of the modern coastal wind systems. >>Obviously, this evolutionary history contradicts ? besides other >>evidences ? the sea level curve for the Younger Holocene as has been >>developed by our Australian colleagues. >>There can be no doubt that the chevrons along the Australian >coastlines >>are special forms worthy to be investigated more intensively. What >>should be done in the near future is to investigate whether these >>chevrons contain sediments too coarse for aeolian transport, and to >>find out, by more radiocarbon dating, whether they were really >>accumulated during the same event. If their genesis from >giant tsunami >>can be confirmed, we have a new instrument for identifying these >>impacts along other coastlines of the world. >>Fig. 14: Possible origin of the West Australian chevrons: not >from the >>distant Réunion volcanic collapse, but from a nearer >submarine slide or >>meteor impact. >>187 >>REFERENCES >>Bryant, E., 2001. Tsunami. The Underrated Hazard. Cambridge >University >>Press. >>Bryant, E.A., Nott, J., 2001. Geological indicators of large tsunamis >>in Australia. Natural Hazards >>24 (3), 231?249. >>Bryant, E., Young, R.W., Price, D.M., 1996. Tsunamis as a >Major Control >>in Coastal Evolution, Southeastern Australia. >>Journal of Coastal Research 12 (4), 831?840. >>Bryant, E. A., Young, R.W., Price, D.M., Wheeler, D.J., 1997. >>The impact of tsunamis on the coastline of Jervis Bay, Southeastern >>Australia. Physical Geography 18 (5), 440?459. >>Hearty, P.J., Neumann, A.C., Kaufman, D.S., 1998. Chevron Ridges and >>Runup Deposits from Storms in the Bahamas Late in Oxygen-Isotope >>Substage 5e. Quaternary Research 50, 309? >>322. >>Kelletat, D., Schellmann, G., 2002. Tsunamis on Cyprus: field >evidences >>and 14C dating results. >>Zeitschrift für Geomorphologie NF 46 (1), 19?34. >>Kindler, P., Strasser, A., 2000. Paleoclimatic significance of >>co-occurring wind- and water-induced sedimentary structures in the >>last-interglacial coastal deposits from Bermuda and the Bahamas. >>Sedimentary Geology 131, 1?7. >>Labazuy, P., 1996. Recurrent landslide events on the >submarine flank of >>Píton de la Fournaise (Réunion Islands). in: McGuire, W.J., Jonas, >>A.P., Neuberg, J., (eds.). >>Volcano instability on the >>earth and other planets. Geological Society of London Special >>Publication 110, 295?306. >>Mastronuzzi, G., Sanso, P., 2000. Boulder transport by catastrophic >>waves along the Ionian coast of Apulia (southern Italy). >Marine Geology >>170, 93?103. >>NGDC ? National Geophysical Data Center, 2001. Tsunami Data at NGDC. >>URL: >>http:// >>www.ngdc.noaa.gov/seg/hazard/tsu.shtml >>Scheffers, A., 2002. Paleo-Tsunamis in the Caribbean: Field Evidences >>and Datings from Aruba, Curacao and Bonaire. Essener Geographische >>Arbeiten 33, Essen, 185 pp. >>Talandier, J., Bourrouilh-Le-Jan, F., 1988. High Energy Sedimentation >>in French Polynesia: Cyclone or Tsunami?. in: >>El-Sabh, M.I., Murty, T.S., (eds.). Natural and Man-Made Hazards. >>Dordrecht, Reidel Publishers, 193?199. >>Science of Tsunami Hazards, Volume 21, Number 3, Page 188 (2003) >> > >--------------------------------------------------------------------- >To unsubscribe, send email to: [EMAIL PROTECTED] >To subscribe, send email to: [EMAIL PROTECTED] >Visit IAGI Website: http://iagi.or.id IAGI-net Archive 1: >http://www.mail-archive.com/iagi-net%40iagi.or.id/ >IAGI-net Archive 2: http://groups.yahoo.com/group/iagi >Komisi Sedimentologi (FOSI) : Deddy >Sebayang([EMAIL PROTECTED])-http://fosi.iagi.or.id >Komisi SDM/Pendidikan : Edy Sunardi([EMAIL PROTECTED]) >Komisi Karst : Hanang Samodra([EMAIL PROTECTED]) Komisi >Sertifikasi : M. Suryowibowo([EMAIL PROTECTED]) Komisi OTODA : >Ridwan Djamaluddin([EMAIL PROTECTED] atau [EMAIL PROTECTED]), >Arif Zardi Dahlius([EMAIL PROTECTED]) Komisi Database >Geologi : Aria A. 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