انڊيمان سمنڊ

**انڊيمان سمنڊ** (Andaman Sea)، تاريخي طور تي برما سمنڊ جي نالي سان پڻ سڃاتو وڃي ٿو، اتر اوڀر هندي سمنڊ جو هڪ حاشيي وارو سمنڊ آهي، جيڪو مرتبان جي نار ۽ ملايا جزيري نما جي اولهه پاسي سان گڏ ميانمار ۽ ٿائيلينڊ جي ساحلي پٽين سان ڳنڍيل آهي ۽ بنگال جي نار کان اولهه ۾ انڊيمان ۽ نڪوبار ٻيٽن سان ڌار ٿيل آهي. ان جو ڏکڻ وارو حصو سماٽرا جي اتر ۾ بريويه ٻيٽ تي آهي ۽ ملاڪا سامونڊي گذرگاهه وڌيڪ ڏکڻ اوڀر ۾ آهي.

روايتي طور تي، سمنڊ کي، ساحلي ملڪن ۽ ان جي مرجاني ريف ۽ ٻيٽن، جيڪا مشهور سياحتي منزلون آهن، جي وچ ۾  مڇي مارڻ ۽ سامان جي نقل و حمل لاءِ استعمال ڪيو ويندو آهي. ڊسمبر 2004ع جي هندي وڏي سمنڊ ۾ سونامي جي ڪري مڇي مارڻ ۽ سياحتي انفراسٽرڪچر کي سخت نقصان پهتو.

## جاگرافي
### جاء
انڊيمان سمنڊ، جيڪو °92 اوڀر کان °100 اوڀر ۽ °4 اتر کان °20 اتر تائين پکڙيل آهي، هندي سمنڊ ۾ هڪ تمام اهم حيثيت رکي ٿو، پر ڊگهي عرصي تائين اڻ کُليل رهيو. ميانمار جي ڏکڻ، ٿائيلينڊ جي اولهه ۽ انڊونيشيا جي اتر ۾، هي سمنڊ بنگال جي نار کان انڊيمان ۽ نڪوبار ٻيٽن ذريعي ڌار ٿيل آهي ۽ انڊو-برمي پليٽ جي حد سان گڏ سمنڊ جي جبلن جي هڪ لاڳاپيل زنجير آهي. ملاڪا سامونڊي گذرگاهه، ملايا جزيري نما ۽ سماٽرا جي وچ ۾، طاس جي ڏکڻ طرف نڪرڻ وارو رستو ٺاهيندو آهي، جيڪو 3 ڪلوميٽر (1.9 ميل) ويڪرو ۽ 37 ميٽر (121 فوٽ) ڊگهو آهي.

### ڦهلائو
بين الاقوامي هائيڊروگرافڪ آرگنائيزيشن "انڊمان يا برما سمنڊ" جي حدن کي هن ريت بيان ڪري ٿو: * ڏکڻ اولهه ۾. هڪ لڪير ("اوئڊجونگ راجا" ["اوجنگ راجا" يا "پوائنٽ راجا"] (5°32′N 95°12′E) کان سماترا ۾ پوئلئي براز (بروئي) تائين. ۽ نڪوبار گروپ جي مغربي ٻيٽن مان. ننڍي انڊمان ٻيٽ ۾ سينڊي پوائنٽ تائين) اهڙي طرح هلندي آهي. ته سڀئي تنگ پاڻي برما سمنڊ سان ملن ٿا. * اتر اولهه ۾. خليج بنگال جي اوڀر واري حد آهي هڪ لڪير (ڪيپ نيگريس (16°03'N) کان برما (ميانمار) ۾. انڊمان گروپ جي وڏن ٻيٽن ذريعي) اهڙي طرح هلندي آهي. ته ٻيٽن جي وچ ۾ سڀ تنگ پاڻي اوڀر طرف آهن.
The International Hydrographic Organization defines the limits of the "Andaman or Burma Sea" as follows:

*On the Southwest.* A line running from *"[[Point Raja|Oedjong Raja]]"* *"Ujung Raja" or "Point Raja"*] () in Sumatra to Poeloe Bras (Breuëh) and on through the Western Islands of the Nicobar Group to Sandy Point in Little Andaman Island, in such a way that all the narrow waters appertain to the Burma Sea.

*On the Northwest.* The Eastern limit of the Bay of Bengal [A line running from Cape Negrais (16°03'N) in Burma Myanmar] through the larger islands of the Andaman group, in such a way that all the narrow waters between the islands lie to the Eastward of the line and are excluded from the Bay of Bengal, as far as a point in Little Andaman Island in latitude 10°48'N, longitude 92°24'E].

*On the Southeast.* A line joining Lem Voalan (7°47'N) in Siam Thailand], and Pedropunt (5°40'N) in Sumatra.

*Oedjong* means "cape" and *Lem* means "point in the Dutch language on maps of the Netherlands East Indies (Indonesia). Lem Voalan [Phromthep Cape] is the southern extremity of Goh Puket (Phuket Island).

### Exclusive economic zone
Exclusive economic zones in Andaman Sea:

### Channels

See Channels in Bay of Bengal, Laccadive Sea, and Arabian Sea.

## ارضيات

The northern and eastern side of the basin is shallow, as the continental shelf off the coast of Myanmar and Thailand extends over  (marked by  isobath). About 45 percent of the basin area is shallower (less than  depth), which is the direct consequence of the presence of the wider shelf. The continental slope which follows the eastern shelf is quite steep between 9°N and 14°N. Here, the perspective view of the submarine topography sectioned along 95°E exposes the abrupt rise in depth of sea by about  within a short horizontal distance of a degree. Isobaths corresponding to  are also shown in the figure to emphasize the steepness of the slope. Further, it may be noted that the deep ocean is also not free from sea mounts; hence only around 15 percent of the total area is deeper than .

The northern and eastern parts are shallower than  due to the silt deposited by the Irrawaddy River. This major river flows into the sea from the north through Myanmar. The western and central areas are  deep. Less than 5% of the sea is deeper than , and in a system of submarine valleys east of the Andaman-Nicobar Ridge, the depth exceeds . The sea floor is covered with pebbles, gravel, and sand.

The western boundary of the Andaman Sea is marked by islands and sea mounts, with straits or passages of variable depths that control the entry and exit of water to the Bay of Bengal. There is a drastic change in water depth over a short distance of , as one moves from the Bay of Bengal (around  deep) to the vicinity of islands (up to  depth) and further into the Andaman Sea. Water is exchanged between the Andaman Sea and the Bay of Bengal through the straits between the Andaman and Nicobar Islands. Out of these, the most important straits (in terms of width and depth) are Preparis Channel (PC), Ten Degree Channel (TDC), and Great Channel (GC). PC is the widest but shallowest () of the three and separates south Myanmar from north Andaman. TDC is  deep and lies between Little Andaman and Car Nicobar. GC is  deep and separates Great Nicobar from Banda Aceh.

### Ocean floor tectonics

Running in a rough north–south line on the seabed of the Andaman Sea is the boundary between two tectonic plates, the Burma Plate and the Sunda Plate. These plates (or microplates) are believed to have formerly been part of the larger Eurasian Plate, but were formed when transform fault activity intensified as the Indian Plate began its substantive collision with the Eurasian continent. As a result, a back-arc basin center was created, which began to form the marginal basin which would become the Andaman Sea, the current stages of which commenced approximately 3–4&nbsp;million years ago (Ma).

The boundary between two major tectonic plates results in high seismic activity in the region (see List of earthquakes in Indonesia). Numerous earthquakes have been recorded, and at least six, in 1797, 1833, 1861, 2004, 2005, and 2007, had a magnitude of 8.4 or higher. On 26 December 2004, a large portion of the boundary between the Burma plate and the Indo-Australian plate slipped, causing the 2004 Indian Ocean earthquake. This megathrust earthquake had a magnitude of 9.3. Between  of the boundary underwent thrust faulting and shifted by about , with the sea floor being uplifted several meters. This rise in the sea floor generated a massive tsunami with an estimated height of  that killed approximately 280,000 people along the coast of the Indian Ocean. The initial quake was followed by a series of aftershocks along the arc of the Andaman and Nicobar Islands. The entire event severely damaged the fishing infrastructure.

### Volcanic activity

Within the sea, to the east of the main Great Andaman island group, lies Barren Island, the only currently active volcano associated with the Indian subcontinent. This island volcano is  in diameter and rises  above sea level. Its recent activity resumed in 1991 after a quiet period of almost 200 years. It is caused by the ongoing subduction of the India plate beneath the Andaman island arc, which forces magma to rise in this location of the Burma plate. The last eruption started on 13 May 2008 and continues. The volcanic island of Narcondam, which lies further north, was also formed by this process. No records exist of its activity.

### Sediments to the Sea
Collectively, the modern Ayeyarwady (Irrawaddy) and Thanlwin (Salween) rivers deliver >600 Mt/yr of sediment to the sea. Most recent studies show: 1) There is little modern sediment accumulating on the shelf immediately off the Ayeyarwady River mouths. In contrast, a major mud wedge with a distal depocenter, up to  in thickness, has been deposited seaward in the Gulf of Martaban, extending to approximately  water depth into the Martaban Depression. Further, 2) There is no evidence showing that modern sediment has accumulated or is transported into the Martaban Canyon; 3) a mud drape/blanket is wrapping around the narrow western Myanmar Shelf in the eastern Bay of Bengal. The thickness of the mud deposit is up to  nearshore and gradually thins to the slope at  water depth, and likely escapes into the deep Andaman Trench; 4) The estimated total amount of Holocene sediments deposited offshore is approximately . If we assume this has mainly accumulated since the middle Holocene highstand (~6000 yr BP) like other major deltas, the historical annual mean depositional flux on the shelf would be  per year, which is equivalent to ~35% of the modern Ayeyarwady-Thanlwin rivers derived sediments; 5) Unlike other large river systems in Asia, such as the Yangtze and Mekong, this study indicates a bi-directional transport and depositional pattern controlled by the local currents that are influenced by tides, and seasonally varying monsoons winds and waves.

## آبهوا ۽ موسم

The climate of the Andaman Sea is determined by the monsoons of southeast Asia, as the prevailing winds reverse with the start of either season. The region experiences north-easterlies with an average windspeed of  from November to February. During these months, the western part of the domain experiences maximum wind intensity. It weakens by March–April and reverses to strong south-westerlies from May to September, with mean wind speeds touching  in June, July, and August, distributed near-uniformly over the entire basin. Wind speeds plummet by October and switch back to north-easterlies from November.

Air temperature is stable over the year at  in February and  in August. Precipitation is as high as /year and mostly occurs in summer. Sea currents are south-easterly and easterly in winter and south-westerly and westerly in summer. The average surface water temperature is  in February and  in May. The water temperature is constant at  at the depths of  and below. Salinity is 31.5–32.5‰ (parts per thousand) in summer and 30.0–33.0‰ in winter in the southern part. In the northern part, it decreases to 20–25‰ due to the inflow of freshwater from the Irrawaddy River. Tides are semidiurnal with an amplitude of up to .

The effect of wind stress on the ocean surface can be explained by wind stress curl. The net divergence of water in the ocean mixed layer results in Ekman pumping. The contrast between the two seasons elicits a very strong negative pumping velocity of more than  per day along the north coast of Indonesia from May to September (shown here, June). This may signify coastal downwelling in the summer. It is also observed that the region develops a weak but positive pumping velocity of less than  per day at the mouth of GC in winter (here, December).

## سامونڊي وهڪري ۽ لهرن جي حرڪيات

Generally, currents are found to be stronger in the south than any other part of the basin. An intense surface outflux through GC, of the order of , occurs during summers and winters. While this flow is directed westwards in winter, it is southwards along the west coast of Indonesia in summer. On the other hand, the TDC has strong surface influx in summer, which weakens by October. This is followed by a sturdy outflux in winter, which wanes by the month of April. Although the surface flow through PC is generally inward during summer monsoon, the preceding and succeeding months experience outflow (strong outflow in October, but weak outflow in April). During April and October, when the effects of local winds are minimal, Andaman Sea experiences the intensification of meridional surface currents in the poleward direction along the continental slope on the eastern side of the basin. This is characteristic of the propagation of Kelvin Waves.

It is observed that the water level rises in the basin between April and November with the maximum rate of piling up of water during April and October (marked by the steep slope of the curve). The rise in sea surface height (SSH) is attributed to rainfall, fresh water influx from rivers, and inflow of water through the three major straits. The first two of these are quantifiable and are hence expressed in volumes of water for comparison. From this, the expected influx through the straits (= SSH anomaly – Rainfall – River Influx) could be deduced. A possible fourth factor, evaporative losses, is negligible in comparison. (Previous studies show that the annual mean freshwater gain (precipitation minus evaporation) of the Andaman Sea is  per year.) It is found that the SSH of the basin is primarily determined by the transport of water through the straits. The contributions from rainfall and rivers become substantial only during summer. Hence, a net inward flow occurs through the straits between April and November, followed by a net outward transport until March.

The basin has a very high rate of transport of water through the straits in April and October. This is a period of equatorial Wyrtki jets, which hit the coast of Sumatra and reflect back as Rossby waves and coastal Kelvin waves. These Kelvin waves are guided along the eastern boundary of Indian Ocean, and a part of this signal propagates into the Andaman Sea. The northern coast of Sumatra is the first to be affected. The  isotherm which deepens during the same period is suggestive of the downwelling nature of Kelvin waves. The waves further propagate along the eastern boundary of the Andaman Sea, which is confirmed by the differential deepening of the 20-degree isotherm along longitudes 94°E and 97°E (averaged over latitudes 8°N and 13°N). These longitudes are chosen so that one represents the western part of the basin (94°E) and the other along the steep continental slope on the eastern side of the basin (97°E). It is observed that both these longitudes experience deepening of the isotherms in April and October, but the effect is more pronounced at 97°E (isotherms deepen by  in April and  in October). This is a concrete signature of downwelling in the basin and is definitely not forced locally as the winds are weaker during this period. This confirms unequivocally that the sudden burst of water into the basin through the straits, the intensification of eastern boundary currents and the coincidental deepening of isotherms in April and October are the direct consequence of the propagation of downwelling Kelvin waves in the Andaman Sea, remotely forced by equatorial Wyrtki jets. The evolution of vorticity in the basin is suggestive of strong shear in the flow during different times of the year, and further indicates the presence of low frequency geophysical waves (such as westward propagating Rossby waves) and other transient eddies.

## ماحوليات

### نباتات

The coastal areas of the Andaman Sea are characterized by mangrove forests and seagrass meadows. Mangroves cover between more than  of the Thai shores of Malay Peninsula whereas seagrass meadows occupy an area of . Mangroves are largely responsible for the high productivity of the coastal waters – their roots trap soil and sediment and provide shelter from predators and nursery for fish and small aquatic organisms. Their body protects the shore from the wind and waves, and their detritus are a part of the aquatic food chain. A significant part of the Thai mangrove forests in the Andaman Sea was removed during the extensive brackish water shrimp farming in 1980s. Mangroves were also significantly damaged by the 2004 tsunami. They were partly replanted after that, but their area is still gradually decreasing due to human activities.

Other important sources of nutrients in the Andaman Sea are seagrass and the mud bottoms of lagoons and coastal areas. They also create a habitat or temporal shelter for many burrowing and benthic organisms. Many aquatic species migrate from and to seagrass either daily or at certain stages of their life cycle. The human activities which damage seagrass beds include waste water discharge from coastal industry, shrimp farms and other forms of coastal development, as well as trawling and the use of push nets and dragnets. The 2004 tsunami affected 3.5% of seagrass areas along the Andaman Sea via siltation and sand sedimentation and 1.5% suffered total habitat loss.

### Fauna

The sea waters along the Malay Peninsula favor molluscan growth, and there are about 280 edible fish species belonging to 75 families. Of those, 232 species (69 families) are found in mangroves and 149 species (51 families) reside in seagrass; so 101 species are common to both habitats. The sea also hosts many vulnerable fauna species, including dugong (*Dugong dugon*), several dolphin species, such as Irrawaddy dolphin (*Orcaella brevirostris*) and four species of sea turtles: critically endangered leatherback turtle (*Dermochelys coriacea*) and hawksbill turtle (Eletmochelys imbricata) and threatened green turtle (*Chelonia mydas*) and olive ridley turtle (*Lepidochelys olivacea*). There are only about 150 dugongs in the Andaman Sea, scattered between Ranong and Satun Provinces. These species are sensitive to the degradation of seagrass meadows.

Coral reefs are estimated to occupy 73,364 rai (117&nbsp;km2) in the Andaman Sea with only 6.4 percent in ideal condition.

## انساني سرگرميون

## پڻ ڏسو

## حوالا

## ٻاهريان ڳنڍڻا
* 
* Myanmar Marine Biodiversity Atlas Online
* 

زمرو:انڊيمان سمنڊ 
زمرو:انڊيمان سمنڊ
زمرو:سمنڊ
زمرو:هندي وڏو سمنڊ
زمرو:ڏکڻ اوڀر ايشيا 
زمرو:بنگال جي نار 
زمرو:ملايا جزيري نما 
زمرو:ايشيا جا سمنڊ 
زمرو:ملائيشيا جا سمنڊ 
زمرو: انڊونيشيا جا سمنڊ 
زمرو:هندستان جا سمنڊ 
زمرو:ٿائيلينڊ جا سمنڊ 
زمرو:ميانمار جا سمنڊ 
زمرو:سماترا جي جاگرافي 
زمرو:ملائيشيا-ٿائيلينڊ حد 
زمرو:هندستان-ميانمار حد 
زمرو:ميانمار-ٿائيلينڊ حد 
زمرو:انڊونيشيا-ٿائيلينڊ حد
زمرو:پٺئين آرڪ بيسن
زمرو:ميانمار جا پاڻي جا ذخيرا 
زمرو:ايشيا جا ماحولياتي علائقا 
زمرو:سامونڊي ماحولياتي علائقا
زمرو:انڊيمان ۽ نڪوبار ٻيٽن جي جاگرافي
زمرو:هندي وڏي سمنڊ ۾ پاڻي جا جسم
زمرو:هندي وڏي سمنڊ جا مارجنل سمنڊ