Hawaiian Island Chain

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The Hawaiian Volcanic Observatory

Hawaii's eight major islands consist of 15 volcanos, the youngest in a chain of more than 129 volcanos (above and below ocean level) stretching approximately 6,100 km across the Northern Pacific. Vulcanoes are younger towards the south-east and the curve in the chain divides the older Emperor Seamount Chain from the younger Hawaiian Ridge.

This is the oldest eruption on the north end of the Kaiser-Seamount chain, 81 million years old. Bending between the two tracks dates back 43 million years. Volcanic activity on the island of Kaua'i ended about 3.8 million years ago, making it the oldest of Hawaii's major islands. The two most frequently erupted volcanos on the island of Hawaii, the youngest of the most important Hawaiian islands, K?lauea and Mauna Loa are the two most actively volcanos in historical terms.

U-boat volume L?'ihi, off the southeast coast of Hawai'i Island, is the youngest of the Hawaiian Ridge vulcano. Each of these volcanos was constructed using an conveyor belt method powered by the movement of plates and a "hot spot" or a heated flag of materials deeply in the ground. Warmth from the Hawaiian hotspot partly smelting shell rocks at a depth of about 200-400 km (125-250 mi) below the earth's crust.

While moving westwards and northwests, each of the volcanoes is moving with it from its original location above the hotspot. Old and new alignment of the chain of volcanoes indicates the Pacific Plate's speed and course. There is a 43 million year old curve between the Hawaiian Ridge and the Kaiser Seamounts, which dramatically changes the way the plates move.

On the basis of the Hawaiian volcanogenic magnetism, researchers have determined an idealised succession of eruptive states for each one. Pre-shield stadium initiating vulcanic activity. U-boat forecourt stadium is the early phase of vulcanic activity, characterised by rare, small-volume outbursts. Kissenlava forms a precipitous vulcanic heap with a flat peak squid and two or three rift zones starting from the peak.

Caldera's evolve and keep filling up during the pre-shielding and shielding phases and go along with the high magma building up the Hawaiian islands. Fissure zone are distinctive characteristics of the Hawaiian volcanos throughout the entire period up to the last eruption phase. Pre-shielding may take 200,000 years, but only a small part of the volcano's end volcanic area.

During volcanic growth, the volcanic ash changes and volcanic outbursts become more common and rich. Once the crossing is completed, the vulcano will enter the phase of plate construction. A recent example of a PRESHELD Stages volume is L?'ihi Seamount. Analytical chemistry of rock gathered during the diving at L?'ihi shows that the eruption progresses to the next phase of uplifting.

All other Hawaiian volcanos bury the precapsule eruptions with subsequent eruptions. Shielding is the most prolific of all the vulcanic eruptions. This is the second and most bulky phase of Hawaiian vulcanism. Over 95 per cent of the Hawaiian Volcan erupts in this phase, which can last up to 2 million years.

In this phase, the Pacific Plate's Oceanian rust, which is not accustomed to the huge mass of volcanos forming on it, is declining sharply - up to 3 mm per year, depending on the actual sink ratios on the island of Hawaii. The early eruption of shields is completely under water, but the growing season is higher than the sink and finally the volcanos appear above the surface.

The Mauna Loa and K?lauea volcanos are in the shelter. It' s not known exactly how long Mauna Loa has been generating lava from shields, but the first streams of shields burst onto the seabed sometime between 0.6 and 1 million years ago. The K?lauea site was replaced by the pre-shield phase about 155,000 years ago.

After the eruption of the shield, an eruption covers the volcanic area. A post shield step covers the vulcano with a tank of volcanos, but these stones make up only a small part of the overall volcanic area. Some Hawaiian volcanos do not pass through this phase (e.g. Ko'olau volcan on Oahu and L?na'i volcano), while other volcanos have broken through thick post shield volcanic regions (e.g. WAIANAE volcan on O'ahu and Mauna Kea volcan on the island of Hawai'i).

Throughout this phase, high columns of molten rock create large quantities of slag and thick, short,'a'? rivers that make the volcanic hillsides steeper as they rise up near peaks and fissure slits. Usually the onset of eruptions drops to zero within 500,000 years during the post shield phase, but this phase can last up to 1 million years.

At the end of the shield phase follows a phase of degradation and settlement, during which gorges can be formed on the sides of the vulcan. Flanking reindeer corals are growing as the vulcanic islets are eroding and decaying. The East Maui's Haleakal? The vulcano started its re-shielding phase about 900,000 years ago.

On Hawaiian Island, Hual?lai and Mauna Kea are also in the post shield phase. Tapered occurrences of eruption on stages usually occur after a long rest time. Forth and last step is the rejuvenation or renewal of volcanic activity. Eruption phases can be accompanied by tapered outbursts, which account for significantly less than 1 per cent of the accumulated eruption volumes of a vulcano.

Coastal igneous flares create vulcanic floods, and continental igneous flares create streams of water flowing through riverbeds (.e.g. M?noa Valley on O'ahu). Rejuvenating stadium activities have low levels of flare-up and can last for several million years. Euptive characteristics on the Ko'olau vulcano on the island of O'ahu are classical samples of a tapered flutter.

One of the most iconical examples is the Diamond Head Crater (L?'ahi in Hawaiian), about 400-500 thousand years old, situated just south of Waik?k? Beach. There are also many lavas on the islands of Kaua'i, Ni'ihau, Moloka'i and West Maui. After the tapering phase, a long phase of degradation and sedimentation finally reduced the volcano island to the surface.

Fundament is a volcanic stone that is easy to erode, especially during the high precipitation in Hawaii. The erosive process includes the slow decomposition due to decomposition and solid mudslides that are displacing large parts of the isles. Most of these landslips can sweep away whole sides of volcanos - such landslips or rubble contaminate the seabed around the Hawaiian isles.

Minor mudslides, especially on the windy, wet sides of the island, are connected to steep erosion gorges or seas. When the volcanos are eroded and the island subsides, they become remnants of remnants of coral atollas, such as those found just westward of La Perouse Pinnacles, the most western and oldest subaeritic remains of a former Hawaiian island.

Once the coral cliffs have died, the reefs are sinking. "Although some volcanos in the Hawaiian Ridge-Emperor Seamounts chain seem never to have grown above the surface, almost all volcanos older than 30 million years are guyotes. The majority of these volcanos were standing at an altitude of several thousand meters above the surface, just like the volcanos that make up today's islets.