Tuesday, December 9, 2008

Partial and Complete Rupture of the Indo-Andaman plate boundary 1847-2004

R. Bilham, E. R. Engdahl, N. Feldl and S. P. Satyabala
University of Colorado, Boulder, CO 80309

We review seismicity along the Nicobar/Andaman plate boundary prior to the Mw=9 earthquake of 26 December 2004, with particular attention to reverse slip in the central and northern parts of the rupture zone 600-1300 km north from the epicenter. Slip is partitioned between convergence and strike-slip motion, which in the northern Andamans is assisted by back-arc spreading. Subduction zone earthquakes prior to the rupture occurred largely to the east, and at deeper depths than the area ruptured in the shallow 2004 megathrust. Large thrust earthquakes in 1847 (Mw>7.5), 1881 (Mw=7.9) and 1941 (Mw=7.7) appear to have occurred on intermediate regions of the down-dip boundary, areas that have been surrounded and probably incorporated into the 2004 rupture. Preliminary reports of 1-4 m of subsidence of the Nicobar islands and 1-2 m uplift of western shorelines of the Andaman islands are consistent with a down-dip fault width of 150-180 km, and a slip of 7-23 m. Based on preliminary reports from the Port Blair tide gage, slip in the Andaman islands, 800 km north of the epicenter, appears to have started no sooner than 36 minutes after the mainshock, some 30 minutes after the primary mainshock rupture is inferred to have arrived from the epicenter, but consistent with large aftershocks occurring in this region 85 minutes after the mainshock, and suggestive of slow slip. The delayed slip was not accompanied by shaking except that from aftershocks.
GPS measurements in the Andaman islands prior to the earthquake indicate a plate convergence rate of 14 mm/year suggesting that great earthquakes with similar slip to the 2004 event cannot occur more frequently than once every 1000 years. A shorter recurrence interval of 400 years is calculated for the epicentral region where convergence rates are higher. The apparent indifference of the 2004 earthquake to the lowered slip deficits caused by previous major earthquakes, and its release of significant seismic moment without evidence for comparable shaking, has implications for the analysis of historical earthquakes in other plate boundaries.


Although there is still some question about the northernmost extent of the primary mainshock rupture in the December 2004 earthquake (Figure 1) aftershocks suggest that it propagated 1300 km from an epicentral region at 3.3degN northwards with a duration of Å10 minutes corresponding to an average propagation velocity of 2.1 km/s (Park et al., 2005). The first 650 km of the rupture appears to be the source zone responsible for the generation of the principal tsunami that resulted in loss of life on remote shorelines Ð sea floor deformation here was rapid compared to the propagation speed of the tsunami (Ortiz, personal communication, 2005). Tsunami run-up on Sumatra and in Thailand locally exceeded 10 m (Borrero, this issue), with a death toll (as of February 2004) of almost 230,000 in the epicentral region, and approximately 70,000 on the distant shorelines of eight nations: Thailand, Sri Lanka, Myanmar, Malaysia, Bangladesh, the Maldives, Kenya, and Somalia. The tsunami's reach extended to the Arctic Ocean via both Pacific and Atlantic pathways. Local peak-to-peak amplitudes of 1 m were recorded on the Pacific coast of Mexico due to focusing of the wave by the East Pacific rise (Ortiz, 2005).

Figure 1A Tectonic setting and earthquake locations in the AndamanÐSumatra region (from Curray et al., 1979,1982) . Rectangles left are historic rupture zones with the 2004 rupture shaded. Open arrows in A indicate plate velocities relative to Asia, double arrows are inferred relative vectors at plate boundaries (Paul et al., 2001). The barbed line is the edge of the accretionary Nicobar-Andaman ridge. The inner line near the trench axis is the -2500 m contour, and the dashed lines left, are locations where alluvial fans have obscured structures on the sea floor. The dashed line linking historic rupture areas passes through the axis of the archipelago. Circles are relocated aftershocks to 14 January and crosses are relocated seismicity 1964-2004 (mostly M³5.5). Star indicates the 26 December 2004 epicenter.

The plate boundary near Nicobar (9degN) changes strike northward from the approximately N20degW strike of the Nicobars, to follow the almost linear N10degE trend of the Andaman Islands for the next 300 km: Little Andaman near 10.7degN, South Andaman at 12deg, Middle Andaman at 12.5deg, and North Andaman at 13.5degN. The timing of the arrival of the tsunami on the east coast of India indicates that no significant tsunami was generated in this northern half of the rupture, indicating that submarine displacements, or rates of slip were smaller north of this 30deg change in strike than to the south.

Analysis of the teleseismically recorded P-waves that terminated primary rupture 9-10 minutes after the origin time, suggests they originated near 12.5±2.5degN (Lomax, 2005), and whereas aftershocks could be resolved teleseismically with 20-30 minutes of the mainshock, aftershocks did not occur at 14degN for more than an hour (Figure 1B). Consistent with an interpretation that slip was slow, and delayed, is the observation that tide gage data from Port Blair suggest (unpublished) record slip developed more than 30 minutes after primary rupture had propagated to the Andaman Islands.

The northward propagation of the rupture passed close to, or through, the rupture zones of major historic earthquakes in 1847, 1881 and 1941, apparently indifferent to the reduced slip potential of these regions. The rupture areas of these early earthquakes are shown to represent less than one third of the down-dip width of the recent earthquake.
We summarize the history of the islands, and geological evidence for their vertical instability. We review seismic evidence for the location of the three major earthquakes that occurred in the two centuries prior to the 2004 earthquake. From preliminary uplift and subsidence data, and relocated seismicity before and following the earthquake, we estimate that reverse slip in the Nicobar Islands (7degN) was more than twice as much as slip in the Andaman islands (12degN).


Although settlement of the Andaman and Nicobar islands occurred many thousands of years ago, indigenous tribes on the islands kept no written records. Ballore (1934), however, notes that the islands native inhabitants revere two deities - the god of storms and the god of earthquakes. The complex role of floods and earthquakes in the beliefs of indigeneous peoples are discussed by Man (1883), Radcliffe-Brown (1922) and Pandya (1995). The Nicobar Islands were known to Ptolemy and were visited by occasional travelers in subsequent centuries, most of whom commented on the inhospitability of the native population: 9th century Arabic traders, Marco Polo c.1292, Jesuits c.1711, Alexander Hamilton c.1727, Viscount Valentia c.1809. The history of damaging earthquakes follows semi-continuous colonial occupation in the mid -18th century by the Danes 1756-68 (Canning et al., 1858; Hamilton, 1828), Moravian Baptists (1768Ð1787), and Austrians (1778Ð1781). Danish administration was re-asserted 1784Ð1837 (Home Department, 1859), and again 1846-1858 (Hunter, 1881) . The death of the Danish king, Christian VIII, brought an end to a century of intermittent Danish rule.

Figure 1B The center panel shows large historical ruptures and their location relative to recent relocated earthquakes (1964-2004) and aftershocks (same symbols as Figure 1A). The panel right illustrates the delay in the initiation of aftershocks in the northern reaches of the rupture zone as a function of the logarithm of time in hours after the mainshock. Aftershock moment release as a function of latitude (left panel) represents a total moment release to mid-February equivalent to a single Mw=7.5 earthquake.

The British administered the Nicobars briefly during the Napoleonic wars 1807Ð1814, and their interest was re-awakened by the loss of a British ship and the alleged murder of its crew by Nicobarese in 1848. Seeking a secure penal colony following the Indian Mutiny they annexed the Nicobar and Andaman islands in 1869 and administered it continuously for the following 76 years, apart for a brief occupation of the islands during the second world war by a Japanese Military administration (23 March 1942 to 6 October 1945).

Colonization of the Andamans occurred first in 1790 with the foundation of a small penal colony (Phillimore, 1945), but by 1796 the settlers and convicts had all perished. Continuous colonial occupation of the Andaman islands did not occur until 1869 following the establishment of a substantial penal colony near Port Blair. Indian administration of the islands has been continuous for the past 60 years.

Geological evidence for vertical motions of the islands

The bathymetry of the Andaman and Nicobar islands were first surveyed in 1770 by Captain Ritchie, and more accurately in 1789 by Captain Blair. Their interiors were explored by a scientific expedition in 1857 that also mapped the Barren and Narcondam volcanoes. The ruins and foundations of the 1789 settlement at Chatham island near Port Blair were described by members of the 1857 expedition as being surprisingly close to sea-level (Figure 2): "The rear wall only was standing, and contained a door and two windows. The remainder of so much of the house as had not been destroyed by the encroachment of the sea, which in this spot must have advanced some 40 or 50 feet, was strewed with large pieces of masonry and brickwork on the beach." [Mouat et al. 1858]. In the same report the expedition noted the shallowness of corals along the western Andamans compared to the deep waters to the west, providing an early hint of the tectonic genesis of the Islands: "These reefs are far more extensive, and form dangers to a far greater distance from the land on the West side than on the East, depths of 100 fathoms being found in many places on the eastern shore within 3 miles of the coast, whereas on the western shore the reefs extend and form dangerous patches at a distance of twenty and twenty-five miles from the land, a fact the probability of which is sufficiently indicated by the geological features of the Islands, the general dip of the stratified rocks being to the eastward at high angle, sometimes as much as 75deg.

Figure 2. Remains of the 1793 settlement on Chatham Island, near Port Blair, from a sketch made on the 1858 expedition. Oldham decided that its near sea-level location was evidence for recent subsidence (Mouat et al., 1858)

Writing in 1884 Oldham concedes that shoreline damage to the early settlement at Port Blair, though possibly caused by marine erosion, supports an observation first made by Kurz (1868) of island subsidence, evidenced by drowned forests in the Nicobars. Oldham provides independent support for recent subsidence through the presence of a similar drowned forest on the NE coast of Havelock Island, 40 km NE of Port Blair. Notwithstanding this evidence for recent subsidence, and another noted by Tipper (1911) near Stewart's Sound (Middle Andaman), Oldham noted the widespread presence of uplifted marine terraces throughout the coast of South Andaman - a raised beach not more than 2-2.6 m above sea level " can be seen forming a terrace, from a few yards to over a mile in width in almost every bay". In places he notes a higher terrace 10-13 m above this lower one. The presence of recent shells on these marine terraces is discussed by Gee (1926).

Figure 3. Localities mentioned in text and fatality data listed by the Andaman and Nicobar Government, 2 March 2005. Elevations of marine terraces identified on SRTM data are identified in parenthesis e.g. (T 18-22 m). Estimates of post-seismic uplift are indicated ±1 m. For only the Indira Point measurement are the data corrected for the tidal range. Note the mean strike of the two island chains differ by approximately 30deg.

In contrast to this evidence for recent subsidence and previous uplift on the eastern margins of the Andamans, Oldham (1885) describes conflicting evidence for coastline stability. Less than 20 km west of Port Blair ancient kitchen middens on the shore require coastal stability for "centuries, if not by tens of centuries". Stoliczka (1881) also describes these kitchen middens and puzzles over this conflicting evidence for stability on some of the islands compared to subsidence and uplift noted in others.

Oldham never visited the Sentinel Islands (40 km west of Port Blair) and although he had been informed that they consisted of uplifted corals, he deduced incorrectly that these western islands were eroded limestone remnants. SRTM data (Figure 3) suggest the presence of at least two coral terraces on North Sentinel Island, at Å25 m and Å50 m elevation. The recent earthquake has raised the island (see Figure 7), a possibility anticipated by Ortiz and Bilham (2003), exposing the fringing reef that formerly surrounded the island. Precise measurements of uplift are unlikely because the island's indigenous population of Sentinelese (Å100) who remained isolated until the last century, will not permit outsiders to approach or land, a policy endorsed by the Indian government.

SRTM imagery of the islands reveals marine terraces at elevations 4-50 m but is inadequate to provide definitive correlations of terraces between islands, or between east and west facing shorelines (Figure 3). In particular SRTM imagery is unable to map the narrow terraces identified by Oldham. Offshore lagoons, however, provide a sufficiently coherent footprint for SRTM imagery. At North Sentinel Island, for example, the newly uplift coral beach can clearly be identifed on the pre-seismic SRTM elevation data.

Nicobar Earthquake 31 October 1847

The first of the three large historical earthquakes in the Andaman/Nicobar region for which we have information occurred in 1847. Following discussions with Nicobar islanders, Hochstetter (1866) reported a "very remarkable earthquake, which is said to have lasted from 31 October to the 5th of December, 1847, on the Nicobar Islands, at which time earthquakes occurred in Java. ...the description of the earthquake seems trustworthy, as I had myself occasion to observe on Kondul the mountain slips referred to in the account ". Kondul island (Kendoel of Montessus De Ballore, 1934) lies between Little Nicobar and Great Nicobar at 7.3degN.

No original account of the 1847 earthquake survives, and all secondary accounts appear to derive from Hochstetter's. The 5 week period of felt aftershocks suggest that its magnitude may have been similar to the 1881 and 1941 earthquakes (7.56.8. Circles are epicenters 1964 to 2004 relocated using methods described in Engdahl et al., (1998). The Sumatra-Nicobar-Andaman earthquake ruptured more than 1300 km of the Indo/Andaman plate boundary (dashed lines) defined by the block of aftershocks recorded to 7 February 2005. The 2004 epicenter is indicated by a star.

The 1941 earthquake is listed in Gutenberg and Richter (1965) as Ms=8.1 and appears even larger in some catalogs, but Pacheco and Sykes [1992] assign it Mw=7.7, similar to the magnitude we derive here. We have relocated its epicenter and although several aftershocks were recorded they have yet to be relocated using secondary phases (Table 2). The preliminary aftershock locations available to this study suggest that rupture may have extended from 250 km north to 50 km south of the mainshock (ignoring the 19 August event). A rupture less than half this length is anticipated from its Mw=7.7 magnitude; we therefore chose to ignore the last two earthquakes listed in Table 2. That is we adopt the weak constraint that the rupture occurred between 11degN and 13degN. Subsidence near and north of Port Blair is consistent with the rupture terminating near the western shoreline of the Andaman Islands. From these scant constraints we infer that slip was less than 3 m on a <50 name="OLE_LINK1">26 June 1941
GMT 11:52:6.63
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27 June 1941

28 June 1941

28 June 1941

30 June 1941
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9 July 1941

14 July 1941
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22 July 1941

10 August 1941
S. of Andamans
19 August 1941
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Earthquakes 1900-2004

In Figure 5 we illustrate the relation between instrumentally recorded earthquakes and the three M>7.5 historical earthquakes discussed above. All M³5.5 earthquakes, and lower magnitude events with Harvard CMT solutions, that have occurred in the past 40 years have been relocated using methods described by Engdahl et al. (1998) with special attention to focal depth. Aftershocks that followed the 2004 earthquake form the block of events at the end of this 150 year interval. Great earthquakes occurred in 1933 and 1861 and adjoin the southern end of the 2004 rupture (Newcomb and McCann, 1987; Zachariasen et al., 1999, 2000; Sieh et al 2004).

The spatial plot of recent earthquakes (Figure 1) reveals the separation between interseismic seismicity mostly to the east of an axis through the archipelago, and aftershocks, mostly to the west, that occur on the shallower surface of the subducting Indian plate. A third population of interseismic and post-seismic earthquakes follow a series of transform and rift earthquakes to the east; these are not discussed in this article article, although we note that their cumulative moment release is much less than the dip-slip earthquakes in the subduction zone to the west.

Cross sections through the Andamans normal to the trend of the trench are consistent with the notion that the 100 km region on the upper surface of the descending Indian plate east of the trench axis was largely aseismic prior to the 2004 earthquake, and that the major earthquakes of 1847, 1881 and 1941 probably ruptured less than one third of the width of the plate boundary that slipped in December 2004 (Figure 6).

Vertical motions 2004

The 26 December 2004 earthquake resulted in widespread adjustments in the elevation of the islands (Figure 3). Post seismic photographs (Giles, 2005) indicate that the Nicobar islands (Å7degN) have sunk 2-4 m. In most cases we do not know the precise time of the photographs and it is thus not possible to estimate the stage of the tide, resulting in an inherent 1 m uncertainty in estimated subsidence or uplift. We quantify the subsidence near the Nicobar Islands from the flooding depth of Katchall and Great Nicobar.

Subsidence of the southernmost tip of Great Nicobar island is 4.25 m as estimated from the January 2005 mean sea-level depression (-0.75 m) of the foundation of the Indira Point lighthouse, that was constructed in 1970, 3.5 m above mean sea level (see Figure 7). In early January, mean sea level relative to the foundation was estimated by eyewitness observations of high and low tide (Office of The Director General Of Lighthouses and Lightships, Andaman & Nicobar, Port Blair, 2005). This large value for subsidence conflicts with later reports where the basis for numerical estimates of subsidence are omitted. For example, the Chief Hydrographer to the Indian Navy B. R. Rao reports the lighthouse subsided 1.4-1.5 m (N. Z. Herald 2 March 2005).

We attempted to estimate the newly flooded depth of water covering shorelines of the Nicobar islands from SPOT images combined with SRTM digital elevation data, but the near-shoreline SRTM imagery proved too inaccurate. Postseismic flooding of Katchall island, however, can be estimated from the change in wavelength of ocean swell waves where they enter Katchal's SW lagoon. SPOT images posted by CNES Singapore before and after the tsunami, show an abrupt decrease in wavelength at the entrance of the lagoon that we assume to be the shoaling of a gravity wave whose speed is proportional to Ãgh. The depth of the lagoon h2 compared to the open water to the SW (h1) is h2=kAh1, where kA is the square of the ratio of deep-water wavelength to shallow-water wavelength, (l1/ l 2)2 , prior to the earthquake. After the earthquake the depth is increased by d, and a new ratio of wavelengths is established kB where h2+d =kB(h1+d). This yields an expression for subsidence, d= h1(kA-kB)/(1- kA). The expression requires the offshore depth to be known and this is available in the form of published bathymetry (Navy, 1943). The method when applied to SPOT images taken on 10 July 2004 and 28 December 2004 yielded a range of values for subsidence, the lowest being 4-7 m. The range is caused both by ambiguity in identifying the fundamental wavelengths in the lagoon, inaccuracies in offshore bathymetry, and departure from horizontal sea-floor conditions. The method is likely to be more successful in open-sea environments, and potentially enables changes in the depths of offshore shoals throughout the Andaman and Nicobar islands to be quantified.
Subsidence of the east coast of Car Nicobar (8degN) evaluated from oblique air photographs and shoreline damage visible in preliminary damage reports (Malek, 2005) appears to be of order 1-2 m, with possible minor uplift (<1 name="OLE_LINK4">0.5-0.8 m. (N.Z. Herald, 2005), and uplift of the western shore of Middle Andaman Island at 12.5degN near Flat Island (Malek, 2005) appears to be approximately 1 m.

These estimates of subsidence and uplift define a neutral axis about which the islands tilted down to the east. This axis constrains the easternmost extent of subsurface rupture, and when used in conjunction with seismic constraints on the dip and location of the subsurface rupture permit us to estimate local reverse slip. Since our vertical constraints are imprecise, based as they are on remotely sensed flooding, or photographs of uplifted corals taken at unknown times of the tidal cycle, our estimates of plate boundary slip are correspondingly uncertain. The models in Figure 6 are based on simple 2-D elastic deformation in a half-space (Savage, 1978) and imply slip of 15-23 m in the Nicobar islands and 5-10 m in the Andaman islands. It is clear that future data from the epicentral region will make estimates of reverse slip considerably more precise, warranting more complex models incorporating deformation associated with a curved plate and with variable coseismic slip.
Figure 7A Historic view of North Sentinel island shoreline (courtesy George Weber) compared to an Indian Coastguard photo after the earthquake. Uplift here is estimated to be 1-2 m with the pre-earthquake coral lagoon now completely raised above mean sea level. Figure 7B are views of Indira Point lighthouse (6deg45.2'N 93deg49.6'E) c. 1980 compared to Indian Coastguard photo of flooded base of lighthouse after the earthquake. Subsidence here is estimated to be 4.25 m based on its foundation being 3.5 m above sea level when constructed, and in January 2005, level with low tide, and submerged 1.5 m at high tide. The steel shell lighthouses, like that at Indira Point, fared well in the earthquake, but masonry lighthouses at Interview Island and Katchall island were badly damaged.

The vertical motions of the islands do not permit constraints on the strike-slip component of rupture, and hence we underestimate total slip. The horizontal co-seismic GPS slip vector reported from Port Blair in a January press release from the Survey of India is 1.15 m to the SE, which is unexpected from considerations of local tectonics. Horizontal displacements of 1-4 m are reported from 12 recovered pre-seismic Survey of India control points in the islands, however, these data are as yet unpublished. Precise constraints of co-seismic GPS displacements of the islands are also anticipated from five locations between 7degN and 14degN conducted by a group of scientists from Trivandrum and Bangalore six weeks before the earthquake, and in the month following the earthquake. At the time of writing these data are unavailable.


We first discuss evidence related to the probability that the primary tsunami was generated in the southern half the primary rupture, and that slip north of approximately 9degN was delayed and occurred more slowly. The 1 Hz P-wave duration of the entire earthquake recorded at worldwide seismic stations is approximately 8 minutes depending on recording azimuth and the confidence with which late arriving P-waves, can be distinguished from S-waves (Park et al., 2005). Directivity shortens the recorded wave-train to the NNW and extends it on stations recording SSE of the epicenter. Moment release peaks in the first 100 seconds, and decays irregularly to insignificance after 600 seconds (Chen Ji, personal communication, 2005). Lomax (2005) notes that the last clearly identifiable P-waves in the wave train are located at approximately 12.5±2.5degN some 480s after the mainshock, implying a mean rupture propagation velocity of 2.3± km/s. If we assume the latest recorded P-wave arrivals corresponds to the northernmost region where aftershocks subsequently developed close to 15degN, we obtain a mean propagation velocity of 2.2 km/s. From the P-wave data we conclude that seismic rupture occurred near Port Blair (11.5deg) at 01:06 GMT (06:36 local time) no later than 8 minutes after the mainshock at 00:58:53 GMT.

The timing of subsidence of 0.25-1.5m at Port Blair is enigmatic. The tide gauge at Port Blair is reported to have recorded initial subsidence of the harbor (or rise in sea level) at 07:14 Indian time, an elapsed interval of 38 minutes after local shaking commenced, consistent with eyewitness accounts of a tsunami arriving 15-30 minutes after 5 minutes of felt shaking. The recorded rise in sea level is too soon for a tsunami to have arrived from the epicenter at 3.3degN, but it may represent a first-arriving positive tsunami from a source near the Nicobar islands. The 1881 tsunami at Port Blair, for example, followed the mainshock by only 14 minutes, suggesting a source area less than 100 km from the harbor, assuming a mean tsunami propagation velocity of Å0.1 km/s (Ortiz and Bilham, 2003). A 38 minute delay requires a tsunami source-region more than 220 km south of Port Blair. The source would need to be close to Car Nicobar at 9.5degN (near piston 26 in Figure 6B of Ortiz and Bilham, 2003), although a deep water tsunami propagation path may permit a source further south.

Tsunami models constrained by the time of the first wave arriving in Vishakapatnan and Chennai on the east coast of India (09:05 and 09:06 local time), suggest that tsunami-genesis was weak north of 7degN (Ortiz, personal communcation, 2005). Had a coherent tsunami been generated north of 8degN these calculations show that it would have arrived at Vishakapatnan earlier than the damaging tsunami generated near the mainshock. We conclude that reverse-slip on the subducting plate north of 9degN was of smaller amplitude or occurred more slowly.

Thus the initial signal on the Port Blair tide gauge may register not subsidence of the harbor, but a positive tsunami surge propagating into the area from the south. A positive initial surge, however, is not expected from locations east of the axis of principal uplift. Detailed modeling is needed to verify this assertion, but such models are unwarranted until the tsunami wave-form data are published. Thus we are uncertain at present whether the initial rise at sea level signifies the first arrival of the tsnunami or subsidence of the harbor; however the observations imply that significant co-seismic subsidence of Port Blair is delayed by at least 36 minutes. Consistent with this observation is the fact that the first recorded aftershock in the Andaman islands did not occur until 83 minutes after the mainshock. This preliminary assessment of the timing of deformation at 10.5degN indicates that substantial slip on the subduction zone beneath the islands followed the initial rupture, and that when it occurred it produced no significant shaking, except as recorded by aftershocks. Subsidence at Port Blair of more than 1 m requires 5-10 m of reverse slip below and west of South Andaman island (Figure 6) and its timing suggests that slip occurred here in the form of accelerated creep, or as one or more slow earthquakes.

Aftershocks suggest that slip occurred on the shallowest 150-170 km width of the plate boundary, a down-dip dimension that is approximately three times wider than the largest earthquakes that occurred in the past century. It would appear, then, that the 2004 rupture enveloped, or re-ruptured, these earlier rupture areas. Paul et al.(2001) estimate from GPS measurements in the 1990's a maximum convergence speed of 14 mm/year between the northern Andamans and the Indian plate. If we assume that this rate has prevailed for the past few centuries the slip deficit prior to the 2004 earthquake in the 1847, 1881 and 2004 rupture zones would have been 2.2, 1.7 and 0.9 m respectively. We do not know for certain whether slip occurred in these regions in 2004, but the mean slip demanded by preliminary dislocation models suggests that substantial additional slip is likely.

Our results have implications for other plate boundaries, where the occurrence of large earthquakes is typically taken to imply a respite from imminent future large earthquakes. For example, Himalayan earthquakes in 1833 (Nepal, Mw=7.7) and 1905 (Kangra Mw=7.8) have hitherto suggested that these regions are unlikely to re-rupture anytime soon. However, both rupture zones are adjacent to, or surrounded by, along-strike and down-dip seismic-gaps where no historical earthquakes have occurred in the past several centuries. This suggests that these historical ruptures could participate in a large future ruptures, and that complacency about future severe seismicity in these regions may be unwarranted. Sieh et al., (2004) note that Sumatran earthquakes also repeat at unexpectedly short intervals.

If large moment release occurs aseismically following great earthquakes it may account for noted discrepancies between long term slip rate and cumulative moment release estimated from seismic data in the historical record. Estimates of cumulative seismic moment in the Himalaya, for example, suggest that the cumulative moment is approximately 30% of that expected from geodetic estimates of convergence (Bilham and Ambraseys, 2005). However, the oblique oceanic convergence of the Andaman plate boundary is structurally and rheologically different from the Himalayan continental collision; one therefore cannot assume strict parallels between seismogenesis in the two regions.

It is not clear how the December 2004 earthquake would have been recorded in the historical record had it occurred many centuries ago. Had it occurred in AD 500 a record of the tsunami would have probably been handed down in mythical terms. Had it occurred in 1600, it would have left a felt intensity record only in Sumatra, and a fragmentary historical record of the tsunami on distant shorelines. Had it occurred in 1800 the tsunami would have been well recorded, and would have been blamed for the damage in the islands as far north as 8degN, but it is doubtful that anyone would have believed the rupture to be longer than 500 km, the length sufficient to account for widespread tsunami run-up. The sparse populations and flexible and transient nature of building styles in the Nicobar and Andaman islands at the time would have left little or no record of shaking. Even now, eyewitness accounts from local residents have left a scant record of shaking intensity, with fewer than two dozen accounts from the >1200-km-long epicentral region with its resident population of 230,000 (Martin, 2005, this volume).

The magnitude of the earthquake suggests that it must be associated with a long recurrence interval. The convergence rate near Port Blair of 12 mm/year (Paul et al, 2001) would require an 800 year renewal time to develop the 10 m apparently released near there in December 2004. Arc-normal convergence rate is slower, with possibly 20% of the convergence velocity partitioned as strike-slip motion to the east of the islands. In contrast the convergence rate near the epicenter is almost four times faster (Sieh et al., 2004), and the renewal time for 20 m of co-seismic slip is of the order of 400 years.


The 26 December rupture appears to have involved slip of the entire plate boundary between 3degN and 15degN, apparently indifferent to the reduced slip prevailing in parts of the plate boundary caused by historical M>7.5 earthquakes. Slip from 3degN to 9degN was Å20 m according to seismic moment estimates (Park et al, 2005) and dislocation models constrained by subsidence estimates near Nicobar island, consistent with the generation of the catastrophic tsunami that damaged remote coastlines. Although primary rupture propagated northward at typical speeds, plate boundary slip north of 9degN developed more slowly, with significant slip manifest not sooner than 36 minutes after the mainshock, according to tide gage data from Port Blair. Slow slip north of 9degN is consistent with the absence of strong recognized tsunami phase at these latitudes, or strong shaking accompanying slip when it occurred. Aftershocks were not recorded in these northern regions for more than 80 minutes after the mainshock, again suggestive of delayed slip.

A pronounced (30deg clockwise) releasing bend in the rupture zone occurs at 9-10degN near the transition between the northern and southern halves of the rupture. The bend occurs at the latitude of the Andaman spreading center that results in the offset of dextral slip on the Andaman transform fault far to the east, and reduces partitioned strike-slip to small values. Thus the change in the dynamics of rupture appears to be associated with an increase in obliquity and a change in the partitioning of strike-slip and reverse-slip northwards.

Slip in the Andaman Islands (10-14degN) not only produced a less damaging tsunami, it occurred in a way that had this event been known only from historically recorded intensities, e.g. from the destruction of Aceh 700 km to the SE along the arc, we are likely to have underestimated its magnitude and rupture area. The absence of intensity data from the mostly submarine region over which its effects were manifest renders the earthquake somewhat unique. Few intensity data are available in the region between 0 and 1200 km west of the epicenter, or the region between 100 and 500 km to the east.

The total reverse slip in the earthquake must be considered tentatitive until more precise field estimates of subsidence are obtained. Preliminary data are consistent with Å20 m of reverse slip in the south decreasing northwards to approximately Å7 m at Port Blair. These displacements correspond to a millennium of cumulative convergence at Port Blair and to approximately half this near the epicenter. The northerly termination of the rupture between the Burmese mainland and the northernmost Andaman Islands has presumably stressed the contiguous part of the plate boundary at 16degN, however, we note that the obliquity of the plate boundary here may be such that strike-slip motion is relative minor and a second 10deg releasing bend here may further facilitate descent of the downgoing plate. The region has been characterized by minor microseismicity in the past century, and it is possible that aseismic processes accommodate reverse-slip on this part of the plate boundary.

Assuming that our estimates of slip are representative of slip throughout the plate boundary (Å20 m for the region from Aceh to the Nicobars, and Å7 m for the Andaman group) we calculate a moment magnitude of Mw=9.1 for the southern 650 x120 km2 of the rupture, and Mw=8.9 for the northern 650x160 km2. These estimates are based on sparse, and in places, conflicting data for uplift and subsidence as noted in this article, and do not account for the strike-slip component of faulting in 2004, however, the total, Mw=9.2, exceeds the NEIC estimate of Mw=9.0 but approaches the magnitude of Mw=9.3 estimated from normal modes (Stein and Okal, 2005).

We thank John Paul, Mike Searle, C.P. Rajendran, Kusala Rajendran, and Vineet Gahalaut for reports from the Andaman Islands in the weeks following the earthquake. Modesto Ortiz has volunteered numerical calculations of the timing of the principal tsunami, despite national demands on his time, when, in the aftermath of the Sumatra/Andaman earthquake, the vulnerability of the Mexican Pacific coastline has assumed significant concern to the Government of Mexico. Chen Ji, and Anthony Lomax kindly shared unpublished data with us and provided numerous insights into rupture propagation. Processed SPOT imagery were accessed on the web site of the Centre for Remote Imaging, Sensing and Processing (CRISP) of the National University of Singapore, http://www.%20crisp.nus.edu.sg/tsunami/tsunami.html. We thank George Weber and the Andaman Association, for permission to reproduce the early photograph of the Sentineli (Figure 7A). Many of the observations for subsidence were obtained in the aftermath of the earthquake from web pages, newspapers and secondary sources without easily accesible citations. Those interested in details are invited to contact the authors. The article has been substantially improved by critical reviews by Dr. Susan Hough, who we thank for numerous suggestions for clarification to the text. We thank NASA for the use of publically available 90 m resolution SRTM imagery. The study was funded by NSF EAR 0003449.

Ballore, M. de (1934), The Seismic Phenomenon in British India and their Connection with its Geology, Mem. Geol. Surv. India, 35(3), 153-194.
Bilham, R., and N. Ambraseys, (2005) Apparent Himalayan slip deficit from the summation of seismic moments for Himalayan earthquakes, 1500-2000, Current Science, in the press.
Borrero, J. (2005) Tsunami survey, this issue.
Canning, C. J., J. Dorin., J. Low and B. Peacock, (1858), Precis of information regarding the Andaman Nicobar and Coco Islands, Home Department Public Consultation Number 33, 2 May 1857, Government of India.
Curray, J. R., F. J. Emmel, D. G. Moore, R. W. Raitt, M. Henry, and R. Kieckhefer, (1979) Tectonics of the Andaman sea and Burma, in Geological and Geophysical Investigations of Continental Margins, edited by J.S. Watkins, L.Montadert, and P.Dickerson, AAPG Mem., 29, 189Ð198.
Curray, J. R., F. J. Emmel, D. G. Moore, and R.W.Raitt, (198). Structure, tectonics and geological history of the NE Indian Ocean, in The Ocean Basins and Margins, vol.6. The Indian Ocean, edited by A.E.M.Nairn and F.G.Sehli, pp.399Ð450, Plenum, NewYork.
Deccan Herald, 16 January 2005, http://www.deccanherald.com/deccanherald/jan162005/n9.asp
Engdahl, E.R., and A. Villasenor (2002), Global Seismicity: 1900-1999, International Handbook of Earthquake and Engineering Seismology, v. 81A, Elsevier Science Ltd., Amsterdam, The Netherlands, pp. 665-690.
Engdahl, E.R., Van der Hilst, R.D., and Buland, R.P., 1997, Global teleseismic earthquake location with improved travel times and procedures for depth determination: Bull. Seism. Soc. Amer, 88(3), 722-743, 1998.
Gee. E. R. (1926) , Geology of the Andaman and Nicobar Islands with special reference to Middle Andaman Island. Rec. Geol. Surv. India, 59, 221.
Giles, D. (2005) Photographs of the Nicobar Islands, http://www.andaman.org/ book/denis_pics/denis.htm
Gutenberg, B. and C. Richter, (1965). Seismicity of the Earth and Associated Phenomena, 2nd Edition, Hafner Publishing Co., New York, NY.
Hochstetter, F, von, (1866). Contributions to the Geology and Physical Geography of the Nicobar Islands, (translated by F. Soliczka) from the "Voyage of the Austrian Frigate Novara, round the world in 1857-1859. Geological Part, Volume 2. 85-112, Vienna, 1866. reproduced in Mem. Geol. Surv. India.4, 59-73, 1870.
Hunter, W.W., The Imperial Gazetteer of India, Trubner and Co., London 1881.
Jhingram, A.G., A note on the earthquake in the Andaman Islands (26June 1941), Rec. Geol. Surv. India, 82(20 300-307, 1953.
Krishnan, R., General Report for 1941, Rec. Geol. Surv. India,,79(1), 193-194,1953.
Kurz, S., (1868) Report on the Vegetation of the Andaman Islands, Government of India, Calcutta 1870.
Lomax, A., (2005) Rapid estimation of faulting extent for large earthquakes by locating the end of the rupture: application to the 2004, Mw=9.0 South Asia megathrust, . Geophysical Research Abstracts, 7, 02543, 2005. Sref-D:1607-7962/gra/EGU05-A-03543 European Geosciences Union, 2005.
Malek, J., et al., (2005) Quick report on the study of the 2004 Sumatra earthquake and tsunami effects, http://www.google.com/search?hl=en&lr=&ie=ISO-88591&q= Kanpur++earthquake
Martin, S., Intensity distribution from the 2004 M9.0 Sumatra-Andaman Earthquake, Seism. Res. Lett., 2005 (This volume)
Man, E. H., On the Aboriginal Inhabitants of the Andaman Islands, (1883). J. Anthropological Institute, 12, 69-175.
New Zealand Herald, 2 March 2005, http://www.nzherald.co.nz/index.cfm?c_id=2&ObjectID=10113068
Mouat, F. J., G. R. Playfair and J. S. Heathcote, (1858) Report by the Andaman Committee to C. Beadon, Secretary to the Government of India, Home Department, dated Port Andaman, 1 Jan 1858
Murty,T.S.,and M.Rafiq, (1991). A tentative list of tsunamis in the Marginal Seas of the North Indian Ocean, Nat. Hazards, 4,81Ð83.
Navy (1943) India Aviation Chart, V3-102, Hydrographic Office, U.S.Navy, Washington
Newcomb,K.R., and W.R. McCann, (1987) Seismic history and seismotectonics of the Sunda Arc, J. Geophys. Res., 92, 421Ð439.
Oldham, R. D. (1885). Notes on the Geology of the Andaman islands, Rec. Geol. Surv. India,18(3) 135-145.
Oldham, R.D. (1884) Note on the earthquake of 31 December 1881, Rec. Geol. Surv. India,17(2) 47-53
Ortiz, M., and R. Bilham, (2003). Source area and rupture parameters of the 31 Dec. 1881 Mw 7.9 Car Nicobar earthquake estimated from Tsunami recorded in the Bay of Bengal, J. Geophys. Res., 108 (B4) 23 April 2003 [2002JB001941RR 2003. ]
Pacheco, J. F., and L. R. Sykes, (1992). Seismic moment catalog of large shallow earthquakes, 1900 to 1989, Bull. Seism. Soc. Amer., 82(3), 1306 - 1349.
Pandya, V., 1994, Recontextualized objects: Andaman Asthetics, Spirits and History, in selected Papers from the 7th Int. Conf. on Hunting and Gathering Societies, Fairbanks. University of Alaska Press.
Park, J, K. Anderson, R. Aster, R. Butler T. Lay and D. Simpson (2005). Global Seismographic Network records the Great Sumatra-Andaman Earthquake, Eos, 86(6),57-64.
Paul, J., Burgmann, R. Gaur, V. K. Bilham, R. Larson, K. M. Ananda, M. B. Jade, S. Mukal, M. Anupama, T. S. Satyal, G., Kumar, D. (2001). The motion and active deformation of India. Geophys. Res. Lett. 28 (4) , 647-651.
Phillimore, R. H., (1945) Historical Records of the Survey of India, Dehra Dun India, 1.
Radcliffe-Brown, A. R., 1922, The Andamese Islanders, a study in social anthropology, 1906. pp. 504.
Savage, J. C., A dislocation model of strain accumulation and release at a subduction zone, J. Geophys. Res., 88, 4984-4996, 1983.
Sieh, K., D. Natawidjaja, M. Chlieh, J. Galetzka and J-P Avouac, 2004, The giant subduction earthquakes of 1797 and 1833, West Sumatra: Characteristic couplets, uncharacteristic slip: in Transactions of the American Geophysical Union abs. 2004
Stein, S., and E. Okal, Ultra-long period seismic moment of the great December 26, 2004 Sumatra earthquake and implications for the slip process, in the press 2005.
Tipper, G. H. (1911) The Geology of the Andaman Islands with reference to the Nicobars, Mem. Geol. Surv. India, 35(4), 195-212.
Valentia, G. (1811) Voyages and Travels to India, Ceylon, the Red Sea, Abyssinia and Egypt in the Years 1802-1806. London: F. C. and J. Rivington, 1811.
Zachariasen, J., K. Sieh, F. Taylor, R. Edwards, and W. Hantoro, 1999, Submergence and uplift associated with the giant 1833 Sumatran subduction earthquake: Evidence from coral microatolls: J. Geophys. Res. 104, 895-919.
Zachariasen, J., K. Sieh, F. W. Taylor, and W. S. Hantoro, Modern vertical deformation above the Sumatran subduction zone: Paleogeodetic insights from coral microatolls, Bull. Seism. Soc. Am.,90,897Ð913,2000.

Tuesday, December 2, 2008

Remembering Kaala Paani - By Swati Dasgupta (Historian)

This is from a Times of India newpaper clipping I had preserved:-
" A tiny uninhabited island in the Andamans with a solar powered lighthouseas its current sole usefulness still bears the name of a knighted general of the East India Company and its successor British administration in India: Hugh Rose. Even the Andaman & Nicobar administration sometimes gets confused about the name. In some maps it is shortened to Rose Island and in some others it is misspelt as Ross island.
What was in British eyes Hugh Rose's lasting claim to fame in India? This General's forces beseiged Rani Laxmibai at Jhansi, pursued her from one battle to another in central India for more than two months and ultimately killed, on June 17,1858, this (by an assessment of her adversaries) bravest and best leader of the Indian Mutiny.
If the national committee set up by the ministry of culture to prepare for a suitable observance of the sesquicentenary of the Great Indian Mutiny or India's First War of Independence accepts the idea of renaming Hugh Rose island it need not fear any objection. The committeee has been stumbling through one controversary to another from its birth. The initial announcement of a budget of Rs 150 Crore for the 150th Anniversary of the uprising appeared hugely extravagant to many who suspected that this was opening a honeypot soon to be infested by corrupt hordes.
Culture minister Ambika Soni hastened to explain that Rs 10 Crore would be sent on the Anniversary of the Mutiny of 1857 and there were other coincidental occasions to celebrate, like the Diamond Jubilee of India's independence and Bhagat Singh's birth anniversary. Nothing much has been heard so far about the programme of celebrations the committee may be drawing up. The anniversaries of the rumblings of the Great Mutiny such as the revolt of the XIX Regiment at Behrampore in Bengal on February 26 and the individual uprising and hanging of Mangal Pandey on March 29 and April 8, dramatised in a film by Aamir Khan, were allowed to pass in silence. One cannot be sure that those in charge will look as far awayas a small island cluster in the Bay of Bengal.
The Andaman and Nicobar administration is reported to have requested only a seminar like the one held at Port Blair during the golden jubilee of India's freedom from the British. The Andamans can claim not too unimportant a place in any programme for remembering the Mutiny and it's aftermath. The notorious Cellular Jail at Port Blair was planned initially for transportation of unbroken fighters for India's freedom to a Dantesque hell. And with sardonic deliberateness the British Indian government named or renamed some of the nearby islands after the soldiers who had crushed the mutineers of 1857. Hugh Rose was one of them. Names like Outram, Havelock, Nicholson, Neil still proclaim from the Andamans the glory of British Generals of an era long bygone. and in an amusing hash cooked by bureaucrats, the recently created Rani Jhansi Marine National Park now cradles the islands named after Outram, John Lawrence and Henry Lawrence. A touristic jewel is known as Havelock, the name of the general who retook Lucknow from Nana Saheb.
Quite incongruously again, a Subhas Mela is held on Havelock every January. Netaji Subhas took symbolic control of Andamans and Nicobar for his Arzi Hukumat Azad Hind, renamed them Shaheed and Swaraj, flew the tricolour at Port Blair and appointed Colonel AD Loganathan of INA as governor of what was called the liberated part of India. The old names came back after World War II. In Indira Gandhi's days Samar Guha tried in the Lok Sabha but failed to revive the names chosen by Netaji Subhas. But Pygmalion Point in Nicobar was renamed Indira Point. Nobody has felt so far any need for taking up the cause of renaming the islands Havelock, Henry Lawrence, John Lawrence, Neill, Outram, Inglis, Sir Hugh Rose, Paget.
The sesquicentenary celebrations are a good occassion to do what should have been done long ago.

Saturday, November 29, 2008

WW II Japanese Machine Gun Bunker in Ross Island.
Reconstuction of Cellular Jail

Ross Island Bazaar

High Tea at Ross Island

Tennis Court at Ross Island

View of Ross Island from Cellular Jail

View of Navy Bay from present day Haddo Jetty

History of Andaman and Nicobar Islands

Ancient History
During the Mauryan empire, especially at the time of Ashoka the great, in mid third century BC there is some mention of A & N Islands being used as a staging area by Indian traders and delegates to the east. Portuguese led the Europeans in their quest to reach the ‘spice islands’ of the far East. The Portuguese came to Nicobar group of Islands, especially the Great Nicobar Island. The place names like Pygmallion Point (now Indira Point), Galathia and Alexandria rivers are a Portuguese legacy. Portuguese used the Southern Islands as a transit point for voyages to India/ Colombo, besides undertaking missionary activities. A reminiscent of their presence is the fusion of quite a few Portuguese words in the Nicobari dialect even today. The Danes (Denmark) remained at Nancowry islands from 1754 to 1779. They controlled the Nicobar Islands and provided support to European ships besides undertaking missionary activities.
The French came to Carnicobar in 1711 to setup a base that could assist their operations against the British for control of the bay. They later withdrew due to unknown reasons.

Name origins
The name Andaman presumably comes from Handuman, which is Malay for the Hindu god Hanuman. The name Nicobar is Malay for land of the naked (people).

First inhabitants
The Andaman and Nicobar islands have been inhabited for several thousand years, at the very least. The earliest archaeological evidence yet docu-mented goes back some 2,200 years; however, the indications from genetic, cultural and linguistic isolation studies point to habitation going back 30,000 to 60,000 years, well into the Middle Paleolithic. In the Andaman Islands, the various tribes maintained their separate existence through the vast majority of time, diversifying into distinct linguistic, cultural and territorial groups. By the 1850s when they first came into sustained contact with outside groups, the indigenous peoples were:
the Great Andamanese, who collectively represented at least 10 distinct sub-groups and languages;
the Jarawa;
the Jangil (or Rutland Jarawa);
the Onge; and
the Sentinelese (most isolated of all the groups).
In total, they numbered around 7,000 at that time. As the number of settlers from the mainland increased (at first mostly prisoners and involuntary indentured labourers, later purposely recruited farmers), these indigenous people lost territory and numbers in the face of land encroachment and epidemics. The Jangil and most of the Great Andamanese groups soon became extinct. Presently, there are only about 400-450 indigenous Anda-manese, the Jarawa and Sentinelese tribes in particular maintaining a steadfast independence and refusing most attempts at contact.
The indigenous people of the Nicobars (unrelated to the Andamanese) have a similarly isolated and lengthy association with the islands. There are two main groups:
The Nicobarese, or Nicobari, inhabiting many of the islands;
The Shompen, restricted to the interior of Great Nicobar.

Geographical Significance
The Andaman and Nicobar Islands are a chain of 572 islands in the Andaman sea. Largest among them, the Andaman Island, is 355 Kms long and 60 Kms wide. The islands are situated approxi-mately 1200 km from India’s eastern seaboard and about 450 km from Malay Peninsula. There was a time when ancient tribes lived here. Some of the natives bear a remarkable resemblance to the aboriginal tribes of Australia. Today some tribes have receded into the deep forest while others have been resettled. Port Blair, it's principal port, is a picturesque and bustling town, full of greenery. It is well connected to the main land by regular passage of ships and scheduled flights from Kolkata and Chennai. Different communities are living in harmony and use Hindi as their language.

British Occupation
Port Blair, the capital of A & N Islands, was named after Lt. Archibald Blair of East India Company. British occupied the Andamans in 1789 as a safe harbour to keep British ships safe and protected in the rains. Due to in inclement weather conditions, outbreak of diseases and the expenses in maintaining the harbour, the British had to abandon the Andamans in 1796. Early in the first decade of the 19th century the roots of the East India Company were firmly entrenched in India. The British were subjecting Indians to a lot of abject atrocities, snatching away land from peasants, destroying the livelihood of craftsmen, increasing taxes, usurping the states from the Nawabs and native kings. Ordinary people, soldiers, nawabs and kings were all being terrified and harassed. Generally everywhere there was resentment and revolt. People were determined to do away with the East India Company.

Recapture of Andaman Islands to keep Political Prisoners
The Andamans reminds us of those freedom fighters who on 10th May 1857, gave the clarion call to rise against the British rule. In January 1858, the British reoccupied Port Blair,
Andamans. For the first time on 10th March 1858, Supdt. J.B. Walker arrived with a batch of 200 freedom fighters. The second batch of 733 freedom fighter prisoners arrived in April 1868 from Karachi. They had been sentenced for life imprisonment. After this however it is not known how many thousands of freedom fighters were sent to the Andamans from the harbours of Bombay, Calcutta and Madras. Their numbers, names and ad-dresses are not known.

The Construction of the Cellular Jail
In 1896, the construction of Cellular Jail started and was completed in 1906 with 698 cells. The Jail had seven wings, spreading out like a seven-petal flower. At the centre was a tower with a turret. Connected to this were the three storey high seven wings with 698 isolated cells. This is why it is called the Cellular Jail.

Horrors Of Prison
The work quotas given to political prisoners were generally impossible to complete within the specified time. Dire punishments were meted out to those who failed to meet them. Punishment was barbaric. Torture and flogging were frequently resorted to on an iron triangular frame, gunny bag uniforms, unhygienic diet, bar fetters, crossbar fetters and neck ring shackles and leg iron and chains were other deterrents for those who refused to submit to the brutal wardens. The punishment varied from handcuffs for a week and fetters for six months to solitary confinement. The freedom fighters brought to the Cellular Jail rebelled against the tyranny of ruthless Jailor David Barrie. Mass hunger strikes were resorted to especially between 1937 and 1938. Three prisoners died. The last hunger strike begun in July 1937 continued for 45 days. The strike was terminated on the intervention of Mahatma Gandhi and Rabindra Nath Tagore. The Government decided to close down the penal settlement and all the political prisoners of Cellular Jail were repatriated to the jails in their respective states in mainland India by January 1938.

Japanese Occupation Of The Islands (1942-45)
The Japanese occupied Andaman and Nicobar Islands during World War II from 23rd March 1942 to 7th October 1945. They put to death hundreds of people in the most bar-baric way, many of them on the mere suspicion of sympathizing with the British. Many educated people were imprisoned in cellular jail as suspected spies and later shot dead. Many were buried in a common grave. The Humfraygunj Martyrs’ Memorial today stands a mute witness to the inhuman treatment meted out to the citizens of India.

Netaji in Andamans
Netaji visited the Andaman Island as a guest of Japanese Government and hoisted the tricolour flag on 30 December 1943. Indian revolutionary freedom fighters were kept in cellular jail , very much like the Bastille in Paris during the French Revolution. Netaji declared that very first bastion to be relieved of the British yoke was Andamans. The British reoccupied the Andaman and Nicobar Islands and re-abolished the Penal Settlement in 1945.

The Demolition of the Cellular Jail.
We do not know on whose initiative the demolition of the Cellular Jail was begun. Indian freedom fighters who were incarcerated in the Cellular Jail and others intervened. We felt strongly that this symbol of tyranny needed to be preserved as a National Memorial to remind our future generations of the tremendous cost that was paid in Indian blood for the freedom of our country.
Cellular Jail-A National Memorial.
After Independence in 1947, many of the erstwhile political prisoners visited the islands. Their association-"Ex-Andaman Political Prisoner’s Fraternity Circle" took up the issue with the Government of India, who accepting this proposal agreed to preserve it as National Memorial without making any substantial change. The Memorial was dedicated to the nation by the then Prime Minister of India on 11th February 1979. Today the entrance block of the National Memorial houses, Photograph Gallery and Museum, displays articles of every day use by the prisoners and method of strict discipline adopted by authorities then in the jail. The first floor of the building has an Art gallery and a Library on Freedom Movement. Netaji Gallery and Old Photographs Gallery has also been set up in the premises of National Memorial. An eternal flame of Freedom - Swatantrya Jyoti has been erected in the vicinity of the Cellular Jail in memory of all freedom fighters and martyrs. An added attraction in the National Memorial is the programme of Light and Sound . This spell-binding show is centered around the wandering spirit of the Cellular Jail which takes the spectators on a historical journey.

Ross Island, erstwhile capital of British penal settlement is named after the British surveyor Reginald Ross. This desolate island was transformed into a thriving township when the British established a penal colony on the Anda-man in the year 1858. Ross Island became the natural choice for the set-tlers due to its commanding geographical location at the mouth of Port Blair harbour, its plentiful supply of fresh water and the security it provided through the water separating it from Port Blair. During those times the settlers went about their business of rec-reating a home far away from home with vigor, so much so that the island soon earned the epithet of ‘The Paris of the East’. In rapid succession rose the Anglican churches, homes for the British and Indian officers, store houses, shops and printing press, hospital, post office, tennis courts, mineral water plant, swimming pool, a bakery, library, general stores. An entire bazaar and three separate clubs were also constructed viz., the Settlement club, the Subordinate club and the Temple club. In all about 500 personnel including officers, troops, Indian merchants and families lived at Ross Island. After almost a century of ruling the islands of Andaman & Nicobar from this tiny ‘island citadel’ the settlers were shaken by a massive earthquake on 26 Jun 1941. The majestic buildings damaged by the earthquake were a sign of events to follow. With the advance of the Japanese forces during World War II, there was also imminent danger to the British settled in the Andaman & Nicobar. Thus the British started withdrawing to mainland and by 1942 Ross Island was virtually deserted. In May 1942 the Japanese forces occupied these Islands. As India gained Independence in 1947 the new government at Port Blair had its hands full administrating and rebuilding the future of the Andaman and Nicobar Islands. The ‘Paris of the East’ now took a back seat and soon turned into a ghost town, the build-ings once throbbing with life now lay dilapidated, engulfed by the tentacles of time. In April 1979 the island was handed over to the Indian Navy, keeping in mind its strategic importance. The Navy over the succeeding years opened Ross Island to visitors and tourists and thus slowly but surely life started to thrive.

Saturday, November 22, 2008

A view of the historic Chatham Saw Mill and Haddo Jetty.

Another view.

Chatham in the foreground and Ross Island behind.

A ferry carrying passangers and vehicles from Chatham to Bamboo Flat.

A view of Ross Island from the Airport Viewpoint.

If you wish to see the Emrald Islands, you need to know the following additional information:-

If you are not a citizen of India, you need to declare your arrival at the airport and produce your travel documents.

If you are travelling around 15 August or 26 January, dont carry pins, batteries, liquids etc in your baggage.

Make alternative arrangements for stay at Kolkata/Chennai in case the flight does NOT take off or return without landing.This is more true during monsoon season. Port Blair airfield gets flooded when it pours heavily. If you are already at Port Blair, make arrangements there.

If you are visiting Baratang Island, you will have to cross Jarawa country.Clicking a single photo of Jarawas can land you in Jail. And it will NOT be the Cellular Jail. Anyway it requires clearance from the administration and hence stick to guided tour.

The Andaman group of inhabited islands are open for tourist stay except for certain specified islands reserved for the aboriginal tribes. Nicobar group is not open for tourism.

You will not be able to do much of snorkelling or recreational diving if you land up between April and November. The summer monsoon morphs into winter monsoon - wind direction changes. In a normal year one can expect 3200 mm of rain.

There is a bed and breakfast concept being introduced by the local tourism department. Since the logistics of sustaining the Islands are difficult, do not expect much in terms of local infrastructure - tourism is in its infancy here.

Do not litter the pristine beaches. Non bio degradable waste is a blasphemy to nature. Plucking Corals is the worst sin one could commit.

Do not expect fresh vegetables to be readily available. Try and stick to seafood - it maybe significantly cheaper. For a veggy meal try the Bay Island resort's Sunday Brunch. It is rewarding for its ambience, breathtaking view and a delicious spread.

Fishes die of old age. Fish and eat.

Sunday, November 16, 2008

View of the World War II origin Port Blair airfield.

The historical Aberdeen Village became the Aberdeen Bazaar of today. Simply referred to as 'Bazaar' by local populace, concrete monstrosities are fast replacing the quaint wooden structures.


Archipelago of 572 islands /islets/rocks comprising 0.2% of landmass of India and 50% of total islands of India.

Bounded by Latitudes 6° N and 14°N, Longitudes 92° E and 94° E which translates into a rectangle of 900 km North to South and 220 km East to West.

Combined area of 8250 sq km approximately. Andaman Group of islands account for nearly 6400 sq km and Nicobar Group accounts for 1850 sq km approximately.

A total of 36 island are occupied, 24 in Andaman Group and 12 in Nicobar Group. However significant human settlement is only in 22 islands.

The islands have International Maritime Boundary Lines (IMBL) running between Landfall island, it’s Northern extremity, and Coco Island of Myanmar (through Coco Channel) and also between Indira Point, it’s Southern extremity, and Banda Aceh, Indonesia, through 6oN channel .The minimum separation from neighbouring, countries across IMBL are as follows:-

* Coco island -42 km

* Banda Aceh -163 km

The islands provide India with approximately 30% of it’s entire Exclusive Economic Zone, i.e., 6 Lakhs sq km. Considering the undersea mineral ,fisheries and hydrocarbon potential of this area, the islands are economically important.

The islands are laid out in a bow shape. The Andaman group has a slight NE to SW alignment and is bounded by Coco channel to the North and Ten Degree channel to the South. It comprises of two administrative districts, i.e., North & Middle Andaman District with District HQ at Mayabunder and South Andaman District with District HQ at Port Blair. The Nicobar group lies between the Ten Degree and Six Degree channels with District HQ at Car Nicobar.

The archipelago is in Seismic Zone 5 (Most Active) with a fault line (extension of Sunda Trench) running parallel and approximately180 nautical miles West of the archipelago. The volcanic belt runs a similar distance East of and parallel to the island chain. The volcanic islands of Narcondum and India’s only active volcano, Barren Island, lie on this belt.

Port Blair is the largest town and main communication centre located equidistant (approx 1200 km) from Kolkata, Vishakhapatnam and Chennai, the three embarkation points for shipping , Air embarkation is only ex Kolkata and Chennai. An international air route does overfly Port Blair. Port Blair is in principle cleared to be upgraded to international airport.

The islands boast of 91% forest cover out of which 11.5% alone is Mangrove forest. The animal kingdom displays a high degree of endemism –nearly 30% of the animal species are endemic.

As per the latest population statistics suitably extrapolated, the island territory has a population of over 4.5 Lakhs , 80% of which is in Andaman Group. The South Andaman district alone has a population of nearly 2.5 Lakhs, of which approximately 1.7 Lakhs are in Port Blair district.

The islands are a ‘Mini-India’ where it’s peculiar style of Hindustani is the spoken language. However the distribution of population by mother tongue is as follows :-

* Bengali - 23%
* Hindi - 20%
* Tamil - 19%
* Telugu - 12%
* Malayalam - 9%
* Nicobari - 8%
* Others - 9%
The distribution of population by religious denomination is as follows:-
* Hindu - 67%
* Christian - 23%
* Muslim - 9%
* Others - 1%

The significant ports in the islands are :-
* Diglipur (North Andaman Island)
* Mayabunder (Middle Andaman Island)
* Port Blair (South Andaman Island)
* Hut Bay (Little Andaman Island)
* Car Nicobar island (Nicobar group)
* Kamorta island (Nicobar group)
* Campbell Bay (Great Nicobar Island)

All airfields/ airstrips in the islands are Defence assets shared for use by civilians.

The islands are home to aboriginal tribes some prized for being the oldest home sapien race on the planet. They are as follows:-
* Great Andamanese. Current population of 43; Negrito stock; originally occupied South Andamans but now restricted to strait Island of Andaman. Access is restricted.
* Jarawa Current population of 240; Negrito stock; and oldest known race; occupy reserves of Middle and South Andaman. Access is restricted.
* Onges. Current population of 97; Negrito stock; occupy areas of Little Andaman. Access is restricted.
* Sentinelese. Current population estimated at 39; Negrito stock; occupy North Sentinel island. Access is DENIED.
* Nicobarese. Current population of about 29.000; Mongoloid stock; population in mainstream and accorded Scheduled Tribe status; occupy all inhabited islands of Nicobar group and own tribal land.
* Shompen. Current population of about 400; Mongoloid stock; occupy area of Great Nicobar Island (GNI). Access is restricted.

With the exception of Nicobarese and Great Andamanese all other tribes are semi nomadic hunter-gatherers.

Though the islands find mention in historical records of up to 18 centuries, the British colonised it in 1857 primarily to establish a penal colony after the Sepoy Mutiny of 1857. The famous Cellular Jail was built in 1906. The islands were captured by the Japanese in 1942 and vacated in 1945 at the end of World War II. The British re occupied it till 1947, when it came to India .

BSNL has a GSM mobile coverage in all large population centres of Andaman and Nicobar groups. A&N telecom Circle has two sub divisions – Andaman (STD Code 03192) and Nicobar (STD Code 03193). Interdialling between the two is by using prefix code ‘95’ instead of ‘0’. BSNL also has WLL networks at Port Blair and Diglipur. Airtel, Vodaphone and Reliance are recent entrants with mobile coverage in Andaman group only.

Saturday, November 15, 2008


Sea journey to Hut Bay, Little Andaman, passing close to Cinque Island and the famed 'Sandbar'.
Ship docked at Hut Bat jetty.

Hut Bay jetty.

State Forest Department Guest House at Hut Bay.

Rate list.

Front view of Guest House.
A Forest Department map of Andaman and Nicobar Islands.

A really rare Green Gecko.

Arecanut drying at the Forest Department Spice farm.

This red eyed fist sized crab was spotted in the rocks of seashore near Hut Bay Bazaar.


A really out of the world and really wild trip would be to the Little Andamans. The crocodile infested waters are the right place for the adventurous. You may even see some out of work elephants and some really thick sawn off trees if you go towards the waterfalls.

Friday, November 14, 2008

Some more snaps of Neil Island

A variety of Sea Cucumber
Lips of a clam

A touch sensitive coral turning silver

A variety of coral


Sea Cucumber

A natural Arch formation


Clam waiting for prey

View of Neil Jetty from the shallowest beach. You can walk nearly 500-600 metres inside without submerging. Walking into the sea is advisable only during rising tide as receding tide tends to pull you inside the sea.