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In this section New Zealand Embassy. Our relationship with Russia New Zealand's relationship with Russia dates back to the 's. Formal connections Trade Embassies Recent official visits The first encounter between Russia and New Zealand occurred in the early 19th century with the imperial Russian expedition to Antarctica led by von Bellingshausen.

Formal connections In addition to formal bilateral contact involving Ministers and senior government officials, New Zealand and Russia engage in a number of regional, multilateral and international organisations, including the United Nations UN where Russia is a permanent member of the Security Council, and New Zealand is a non-permanent member, for Measles outbreak in New Zealand 26 Sep Europe.

Measles outbreak in New Zealand 25 Sep Africa. Find out more about the current outbreak of measles in New Zealand. Mount Egmont is a huge, conical, andesite volcano, with the remnants of two other volcanic cones nearby; all are of Pleistocene age. In the Waikato there are eroded Pleistocene cones of approximately basic andesite composition. The largest is Pirongia, some m high.

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Auckland city and the area immediately to the south has been the scene of many eruptions of basalt lava and scoria in late Pleistocene and Holocene times; and many small scoria cones can be seen in the locality. Late Tertiary and Quaternary basaltic eruptions in North Auckland have built lava plateaus and many young cones. Earthquakes are most common in certain geographically limited regions, one of which includes New Zealand. Within these disturbed zones, young fold mountains, oceanic trenches, volcanoes, anomalies in the Earth's gravitational field, and active geological faulting are also usual, and like the earthquakes have their ultimate cause in the internal processes incidental to the major structural development of the Earth, and as yet imperfectly understood.

The seismically active zones define the margins of a system of stable blocks or plates which are not completely inactive, but experience large earthquakes only infrequently, and are thought to be the primary units of the Earth's crust. Two of these units, the Pacific and Indian Plates, abut in the vicinity of New Zealand, forming a triple junction with a third, the Antarctic Plate, south of Macquarie Island. As a result of thermally generated convective movements in the deeper levels of the earth, relative displacement of the plates is occurring and this provides the continuing source of the energy that is intermittently released as earthquakes.

Instrumental records have shown that at the time of an earthquake large shearing movements take place at the source.

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It seems probable that all major earthquakes are the result of the breakage of rock under strain, but other factors such as the presence or absence of liquid in the pores and fractures of the rock are also of primary importance in determining the time and place at which a shock occurs. In large shallow earthquakes a rupture may appear at the surface, forming or renewing movement on a geological fault. In regions where the majority of earthquakes are very shallow, such as California, there is a tendency for the earthquake origins to cluster near geological fault traces, but in regions where there is deeper activity, such as New Zealand, this is not so.

For example, there is little activity near the Alpine Fault, which stretches for some km from Milford Sound to Lake Rotoiti, and is considered one of the world's largest and most active faults. Conversely, instances of fault movement that have not been accompanied by earthquakes are known. Practical assessments of earthquake risk must therefore be based upon the statistics of known earthquake distribution and the broader geological setting of the origins.

New Zealand Seismicity —Compared with some other parts of the Pacific margin, such as Japan, Chile, and the Philippines, the level of seismic activity in New Zealand is moderate. It may be roughly compared with that prevailing in California. A shock of Richter magnitude 6 or above occurs on the average about once a year, one of magnitude 7 or above once in ten years, and one of about magnitude 8 perhaps once a century, but in historic times only one shock the south-west Wairarapa earthquake in is known to have approached this magnitude.

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Other natural disasters and accidents are together responsible for more casualties than earthquakes, the most serious seismic disasters in New Zealand having been the Hawke's Bay earthquake of in which deaths occurred, and the Buller earthquake of in which there were The total resulting from all other shocks since is less than 15 deaths.

The last earthquake to cause deaths occurred at Inangahua in , when 3 people died. Regarded broadly, the zone of seismicity within which New Zealand lies extends continuously from the triple junction south of Macquarie Island to Samoa. When looked at more closely, breaks in continuity and changes in the character of the activity become apparent. There are changes in direction, in the positional relationship of the deeper and shallower activity, and in its association with the other geophysical and geological features of the region.

Within New Zealand itself, at least two separate systems of seismic activity can be distinguished. Less clearly defined activity covers the remainder of the two main islands, and extends eastwards from Banks Peninsula to include the Chatham Islands. Shallow earthquakes, which are the most numerous, originate within the Earth's crust, which in New Zealand has an average thickness of some 35 km.

These shocks are responsible for almost all damage to property, and now and in the past they have been widely scattered throughout the country. In historically recent times, the Main and Fiordland Seismic Regions have been significantly more active than the rest of New Zealand, but neither the Central Seismic Region that lies between them nor the Northland peninsula has been free from damaging shocks. The details of the present pattern are not necessarily unchanging, and could alter significantly after the occurrence of a major earthquake. Because of this, because of the broader geophysical setting, and because of the distance to which the effects of a large earthquake extends, it would be highly imprudent to treat any part of New Zealand as free from the risk of serious earthquake damage.

Many active regions of the Earth have only shallow earthquakes, but in others shocks have been known to occur at depths as great as km below the surface. It is thought that these deep shocks originate within the edges of crustal plates that have been drawn down or thrust beneath their neighbours. Such deep events are common in both the Main and Fiordland Seismic Regions of New Zealand, but their relative positions with respect to the shallow activity and to other geophysical features are rough mirror images.

This is believed to indicate that in the North Island, the edge of the Pacific Plate lies below that of the Indian Plate, while in the south of the South Island the Pacific Plate is uppermost and the Indian Plate has been thrust beneath it. The most important system of deep shocks in New Zealand lies in a well-defined zone beneath the Main Seismic Region, stretching from the Bay of Plenty to Nelson and Marlborough. The maximum depth of occurrence is about km at the northern end, and decreases smoothly to a depth of about km before the southern boundary of the region is reached.

Along the whole of the system, there is also a decrease in maximum depth from west to east. In northern Taranaki, near the western limit of this activity, a small isolated group of shocks at a depth of about km has also been recorded. In the Central Seismic Region only shallow shocks are known. The maximum depth of the earthquakes in the Fiordland Region appears to be only about km, but it is only recently that instrumental coverage has been adequate for a proper study of this area. Here, the deep activity is more concentrated than in the north, lying close to Lakes Te Anau and Manapouri.

Both earthquakes and volcanoes are found in geophysically disturbed regions, but although small earthquakes usually accompany volcanic eruptions, large ones are rare. Regions of active volcanism are also subject to periodic outbreaks of small earthquakes, all of similar magnitude, and very numerous. Although the number of shocks may cause alarm, it is unusual for even minor damage to result. There is not often a simultaneous volcanic outbreak, but swarms do not seem to occur in non-volcanic regions.

In New Zealand they have occurred in the volcanic zone that includes Mt. Seismological Observatory —Each year the Seismological Observatory, Wellington, a section of the Geophysics Division of the Department of Scientific and Industrial Research, publishes the analyses of many hundred earthquakes originating in the New Zealand region, using data obtained from its own network of recording stations, and from stations in other countries.

The instrumental data are supplemented by information about felt effects, supplied by a large number of voluntary observers, who complete a standard questionnaire.

The network of recording stations controlled by the Observatory is now one of the world's largest and most extended, covering the main islands of New Zealand, a large part of the south-west Pacific, and the Ross Dependency. The 35 permanent stations now operating are:. At Afiamalu, Rarotonga, Wellington, and Scott Base the equipment includes instruments of internationally standardised pattern designed to record both local and distant activity. The stations at Karapiro and Roxburgh are also equipped to record both local and distant shocks.

At the other stations, many of which record more than one component of the ground motion, the instruments are primarily intended for the study of shocks within about km. Scott Base and several of the island stations provide preliminary readings by radio, but all final analyses are made at the Observatory in Wellington. Two networks of more closely-spaced stations, connected to central recorders by radio links or land lines, provide for detailed studies of small earthquakes in particular regions. One, for general research purposes, is centred on Wellington, and the other, near Lake Pukaki in the South Island, is primarily intended to monitor any change in earthquake activity associated with the development of a hydroelectric power scheme.

These networks also provide valuable readings of New Zealand and overseas earthquakes.

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Portable equipment is available for more intensive study of aftershock sequences, earthquake swarms, and micro-earthquakes, and for other research projects. In addition, the Department's Physics and Engineering Laboratory maintains a network of strong-motion recorders intended to provide data on large shocks for engineering purposes.

The information collected and published by the Observatory covers all significant earthquakes in the New Zealand region. It is made freely available to the public and the press, as well as to seismologists, engineers, and other specialists.

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In addition, a very large number of distant earthquakes are recorded, and readings of these, as well as of the local activity, are regularly sent to international agencies and to overseas seismologists who have a need for them. The Observatory itself carries out a vigorous programme of research into problems of seismicity and earthquake mechanism, and into the structure and constitution of the Earth's crust and its deep interior. There was no significant damage, and only two shocks were felt over wide areas. No shock reached magnitude 6, and there was less than half the usual number of shocks reaching magnitude 5.

Although the Seismological Observatory located and assigned magnitudes to some small events, this was about less than in a normal year. On the morning of May 15 some minor damage resulted from a shock of magnitude 3. A hopper at the Ruawai lime-works fell and hit an adjoining building, and in a few places where local soil conditions intensified the vibration, plaster and brickwork was slightly cracked.

This part of New Zealand is widely believed by the public to be free from earthquake risk, and it is unusual for damage to result from so small a shock. This may be possibly attributed to the failure of local builders to consider the need for earthquake resistance, and to the unusually shallow origin of the shock. The largest shock within the New Zealand region proper was a shallow earthquake of magnitude 5. Although it was felt over much of north Canterbury and Westland, the shaking was nowhere severe enough to move goods or cause damage.

The only other event of comparable size was a deep event of magnitude 5. It was centred some km beneath the western Bay of Plenty and attracted attention in many places from Tolaga Bay to Blenheim. It was not, however, felt in places near the epicentre, the felt area being displaced to the east by the structural peculiarities of the North Island.