ارجو المساعدة عاجل

السلام عليكم اخواني
انا محتجة مساعدتكم في بحث مادة الانجليزية السنة 2 للوحدة رقم 6 "no man is in island"
ارجو انكم تساعدوني في الاسءلة الي ممكن اطرحها
ارجو مساعدتكم ضروري

السلام عليك اختى تاكدى انه في هدا المنتدى ادا ما احتاج احادنا الى شيئ سيلبيه اخوة بسرعة وبصدر رحم وتاكدى اننا لن نبخل عليك اختاه

السلام عليكم
مرحبا بيك اختي كيف حالك
أولا أختي لم أفهم ما تريدينه بالتحديد في خصوص بحثك
لكن سأحاول البحث عنه اضافة الى هذا أختي وجميع من في المنتدى اريد منكم مساعدتيفي جلب أكبر عددممكن منالدروس والحوليات الاصة بالبكالوريا لصالح طلابنا
وأتمنى التوفيق للجميع
ومن لديه أي مشكل ليراسلني

السلام عليك اخى رؤووف انا لدي كثر من الاشياء النافعة والقيمة حاولت مرارا وتكرا المشاركة بها لتعم الفائدة لطلاب القسم النهائى لكن بصراحة دون جدوى لم اعرف لدي مواضيع مع الحلو ادا تكرمت واخبرتنى الطريقة بكل فرح وسروح سوف اشارك بها بل هدا واجب منى وفرض

مرحبا أخت نسمة
بخصوص الشرح
أمهليني بعض الوقت وساوافيكم بشرح بالفيديو
هكذا أفضل

هذا شرح مرفق بالصورة
أرجو ان يكون كافي
ارجو المساعدة عاجل View

اهلا اختي دليلة هل انت بحاجة الي اجوبة عن اسئلة لك ام انه طلب منك اسئلة تخص هذه الوحدة ؟؟ اسفة اختي لم افهم مطلوبك هلا توضحي اكثر واتاكدي انو دائما نحاول نساعدو كل من يطلب مساعدة لانو واجب علينا كاخوة
انتظر ردك

هذه الصورة كشرح

شكرا على حسن استجابتكم لطلبي
و انا رح اكتب المطلوب لكم و اتمنى انكم تساعدوني
و اذا كان في عضو يدرس في السنة 2ثانوي علمي اتمنى منه انه يروح على الصفحة 132و هي فيها تفاصيل البحث
و اذا ما قدرتو ماعليش و نشكركم على مجهودك

البحث يتكلم عن الكوارث الطبيعية بالانجليزية مثل الفيضان . الزلازل. البراكين و غيرها
و المطلوب مني هو اني نقوم استجواب (استبيان) يعني اني نطرح مجموعة من الاسئلة على الناس كنطرح عليهم سؤال what do you think about earthquakes?
و هيك اسئلة من هذا القبيل
و انا محتاجة تساعدوني نجد هذي الاسئلة لي ممكن نطرحها هذي المرحلة 1
2 نقوم بمقابلة مع شخص من الاشخاث لي طرحت عليهم اسئلتي بخصوص كارثة طبيعية يعني ندير حوار معاه نطرح عليه الاسئلة و هو يجاوبني
3 جمع البيانات كاملة اي الاسئلة و الاجوبة
4 تقرير مع الرسم البياني اي اني نمثل النسب في دائرة نسبية او مدرج.....
5 مجموعة من التعليمات حول السلامة من الكوارث الطبيعية
6 تدكير لكيفية التعامل الناس مع مثل هذه الكوارث في الخارج

و هذا هو البحث لي راه مقلقني كاين بعض المراحل لي نقدر نديرهم روحي مثل 2 3 4 5 6

خصني الاسئلة فقط تساعدوني في ايجادها
نتمنى ما نكونش قلقتكم معاي و كل شخص حاول انه يساعدني و لو بالقليل مشكور
ممكن انكم تطرحو الاسئلة بالعربية و انا نطرجمها
سامحوني اذا ازعجتكم

السلام عليكم مافي ازعاج ولا اي شيء اختي من دواعي سرورنا انو نقدمو ولو القليل من المساعدات
مااول شيء يخطر ببالك عندما تسمع ب كلمة الزلزال؟
What is the first thing that comes to mind when you hear the word of an earthquake?

ماهو اخر بلد حدث فيها زلزال؟
What is another country where the earthquake occurred ؟

كيف يحدث الزلزال؟
How is earthquake? ؟

ماهي اسباب حدوثه؟
What are the reasons it occurs ؟

ماهي الخسائر المترتبة عن حدوثه؟
What are the implications for the losses happen?

هل يمكن التنبؤ بحدوثه؟ وكيف؟
Can you predict to happen and how?

اسفة حبيبتي هذه القليل من الاسئلة لدي رجوع للموضوع محاولة الحصول على عدد كبير من الاسئلة

شكرا اخى رؤوف ولك كل الوقت

السلام عليكم الأخت دليلة ـ اتمنى أني وفقت في بحثي

اضغط على الرابط

http://www.idahogeology.org/FieldWorkshops/BorahPeak2005/Student%20Presentations/Earthquake%20Curriculum.pdf

*******************************

Naturally occurring earthquakes

Fault types
Tectonic earthquakes occur anywhere in the earth where there is sufficient stored elastic strain energy to drive fracture propagation along a fault plane. In the case of transform or convergent type plate boundaries, which form the largest fault surfaces on earth, they move past each other smoothly and aseismically only if there are no irregularities or asperities along the boundary that increase the frictional resistance. Most boundaries do have such asperities and this leads to a form of stick-slip behaviour. Once the boundary has locked, continued relative motion between the plates leads to increasing stress and therefore, stored strain energy in the volume around the fault surface. This continues until the stress has risen sufficiently to break through the asperity, suddenly allowing sliding over the locked portion of the fault, releasing the stored energy. This energy is released as a combination of radiated elastic strain seismic waves, frictional heating of the fault surface, and cracking of the rock, thus causing an earthquake. This process of gradual build-up of strain and stress punctuated by occasional sudden earthquake failure is referred to as the elastic-rebound theory. It is estimated that only 10 percent or less of an earthquake's total energy is radiated as seismic energy. Most of the earthquake's energy is used to power the earthquake fracture growth or is converted into heat generated by friction. Therefore, earthquakes lower the Earth's available elastic potential energy and raise its temperature, though these changes are negligible compared to the conductive and convective flow of heat out from the Earth's deep interior.[2]
Earthquake fault types
Main article: Fault (geology)
There are three main types of fault that may cause an earthquake: normal, reverse (thrust) and strike-slip. Normal and reverse faulting are examples of dip-slip, where the displacement along the fault is in the direction of dip and movement on them involves a vertical component. Normal faults occur mainly in areas where the crust is being extended such as a divergent boundary. Reverse faults occur in areas where the crust is being shortened such as at a convergent boundary. Strike-slip faults are steep structures where the two sides of the fault slip horizontally past each other; transform boundaries are a particular type of strike-slip fault. Many earthquakes are caused by movement on faults that have components of both dip-slip and strike-slip; this is known as oblique slip.
Earthquakes away from plate boundaries
Main article: Intraplate earthquake
Where plate boundaries occur within continental lithosphere, deformation is spread out over a much larger area than the plate boundary itself. In the case of the San Andreas fault continental transform, many earthquakes occur away from the plate boundary and are related to strains developed within the broader zone of deformation caused by major irregularities in the fault trace (e.g., the “Big bend” region). The Northridge earthquake was associated with movement on a blind thrust within such a zone. Another example is the strongly oblique convergent plate boundary between the Arabian and Eurasian plates where it runs through the northwestern part of the Zagros mountains. The deformation associated with this plate boundary is partitioned into nearly pure thrust sense movements perpendicular to the boundary over a wide zone to the southwest and nearly pure strike-slip motion along the Main Recent Fault close to the actual plate boundary itself. This is demonstrated by earthquake focal mechanisms.[3]
All tectonic plates have internal stress fields caused by their interactions with neighbouring plates and sedimentary loading or unloading (e.g. deglaciation[4]). These stresses may be sufficient to cause failure along existing fault planes, giving rise to intraplate earthquakes.[5]
Shallow-focus and deep-focus earthquakes
The majority of tectonic earthquakes originate at the ring of fire in depths not exceeding tens of kilometers. Earthquakes occurring at a depth of less than 70 km are classified as 'shallow-focus' earthquakes, while those with a focal-depth between 70 and 300 km are commonly termed 'mid-focus' or 'intermediate-depth' earthquakes. In subduction zones, where older and colder oceanic crust descends beneath another tectonic plate, deep-focus earthquakes may occur at much greater depths (ranging from 300 up to 700 kilometers).[6] These seismically active areas of subduction are known as Wadati-Benioff zones. Deep-focus earthquakes occur at a depth where the subducted lithosphere should no longer be brittle, due to the high temperature and pressure. A possible mechanism for the generation of deep-focus earthquakes is faulting caused by olivine undergoing a phase transition into a spinel structure.[7]
Earthquakes and volcanic activity
Earthquakes often occur in volcanic regions and are caused there, both by tectonic faults and the movement of magma in volcanoes. Such earthquakes can serve as an early warning of volcanic eruptions, as during the Mount St. Helens eruption of 1980.[8] Earthquake swarms can serve as markers for the location of the flowing magma throughout the volcanoes. These swarms can be recorded by seismometers and tiltmeters (a device that measures ground slope) and used as sensors to predict imminent or upcoming eruptions.[9]
Rupture dynamics
A tectonic earthquake begins by an initial rupture at a point on the fault surface, a process known as nucleation. The scale of the nucleation zone is uncertain, with some evidence, such as the rupture dimensions of the smallest earthquakes, suggesting that it is smaller than 100 m while other evidence, such as a slow component revealed by low-frequency spectra of some earthquakes, suggest that it is larger. The possibility that the nucleation involves some sort of preparation process is supported by the observation that about 40% of earthquakes are preceded by foreshocks. Once the rupture has initiated it begins to propagate along the fault surface. The mechanics of this process are poorly understood, partly because it is difficult to recreate the high sliding velocities in a laboratory. Also the effects of strong ground motion make it very difficult to record information close to a nucleation zone.[10]
Rupture propagation is generally modelled using a fracture mechanics approach, likening the rupture to a propagating mixed mode shear crack. The rupture velocity is a function of the fracture energy in the volume around the crack tip, increasing with decreasing fracture energy. The velocity of rupture propagation is orders of magnitude faster than the displacement velocity across the fault. Earthquake ruptures typically propagate at velocities that are in the range 70–90 % of the S-wave velocity and this is independent of earthquake size. A small subset of earthquake ruptures appear to have propagated at speeds greater than the S-wave velocity. These supershear earthquakes have all been observed during large strike-slip events. The unusually wide zone of coseismic damage caused by the 2001 Kunlun earthquake has been attributed to the effects of the sonic boom developed in such earthquakes. Some earthquake ruptures travel at unusually low velocities and are referred to as slow earthquakes. A particularly dangerous form of slow earthquake is the tsunami earthquake, observed where the relatively low felt intensities, caused by the slow propagation speed of some great earthquakes, fail to alert the population of the neighbouring coast, as in the 1896 Meiji-Sanriku earthquake.[10]
Earthquake clusters
Most earthquakes form part of a sequence, related to each other in terms of location and time.[11] Most earthquake clusters consist of small tremors that cause little to no damage, but there is a theory that earthquakes can recur in a regular pattern.[12]
Aftershocks
Main article: Aftershock
An aftershock is an earthquake that occurs after a previous earthquake, the mainshock. An aftershock is in the same region of the main shock but always of a smaller magnitude. If an aftershock is larger than the main shock, the aftershock is redesignated as the main shock and the original main shock is redesignated as a foreshock. Aftershocks are formed as the crust around the displaced fault plane adjusts to the effects of the main shock.[11]
Earthquake swarms
Main article: Earthquake swarm
Earthquake swarms are sequences of earthquakes striking in a specific area within a short period of time. They are different from earthquakes followed by a series of aftershocks by the fact that no single earthquake in the sequence is obviously the main shock, therefore none have notable higher magnitudes than the other. An example of an earthquake swarm is the 2004 activity at Yellowstone National Park.[13]
Earthquake storms
Main article: Earthquake storm
Sometimes a series of earthquakes occur in a sort of earthquake storm, where the earthquakes strike a fault in clusters, each triggered by the shaking or stress redistribution of the previous earthquakes. Similar to aftershocks but on adjacent segments of fault, these storms occur over the course of years, and with some of the later earthquakes as damaging as the early ones. Such a pattern was observed in the sequence of about a dozen earthquakes that struck the North Anatolian Fault in Turkey in the 20th century and has been inferred for older anomalous clusters of large earthquakes in the Middle East.[14][15]
Size and frequency of occurrence

There are around 500,000 earthquakes each year. About 100,000 of these can actually be felt.[16][17] Minor earthquakes occur nearly constantly around the world in places like California and Alaska in the U.S., as well as in Guatemala. Chile, Peru, Indonesia, Iran, Pakistan, the Azores in Portugal, Turkey, New Zealand, Greece, Italy, and Japan, but earthquakes can occur almost anywhere, including New York City, London, and Australia.[18] Larger earthquakes occur less frequently, the relationship being exponential; for example, roughly ten times as many earthquakes larger than magnitude 4 occur in a particular time period than earthquakes larger than magnitude 5. In the (low seismicity) United Kingdom, for example, it has been calculated that the average recurrences are: an earthquake of 3.7 - 4.6 every year, an earthquake of 4.7 - 5.5 every 10 years, and an earthquake of 5.6 or larger every 100 years.[19] This is an example of the Gutenberg-Richter law.

The Messina earthquake and tsunami took as many as 200,000 lives on December 28, 1908 in Sicily and Calabria.[20]
The number of seismic stations has increased from about 350 in 1931 to many thousands today. As a result, many more earthquakes are reported than in the past, but this is because of the vast improvement in instrumentation, rather than an increase in the number of earthquakes. The United States Geological Survey estimates that, since 1900, there have been an average of 18 major earthquakes (magnitude 7.0-7.9) and one great earthquake (magnitude 8.0 or greater) per year, and that this average has been relatively stable.[21] In recent years, the number of major earthquakes per year has decreased, though this is probably a statistical fluctuation rather than a systematic trend. More detailed statistics on the size and frequency of earthquakes is available from the United States Geological Survey (USGS).[22] Alternatively, some scientists suggest that the recent increase in major earthquakes could be explained by a cyclical pattern of periods of intense tectonic activity, interspersed with longer periods of low-intensity. However, accurate recordings of earthquakes only began in the early 1900s, so it is too early to categorically state that this is the case.[23]
Most of the world's earthquakes (90%, and 81% of the largest) take place in the 40,000-km-long, horseshoe-shaped zone called the circum-Pacific seismic belt, known as the Pacific Ring of Fire, which for the most part bounds the Pacific Plate.[24][25] Massive earthquakes tend to occur along other plate boundaries, too, such as along the Himalayan Mountains.[26]
With the rapid growth of mega-cities such as Mexico City, Tokyo and Tehran, in areas of high seismic risk, some seismologists are warning that a single quake may claim the lives of up to 3 million people.[27]
Induced seismicity

Main article: Induced seismicity
While most earthquakes are caused by movement of the Earth's tectonic plates, human activity can also produce earthquakes. Four main activities contribute to this phenomenon: storing large amounts of water behind a dam (and possibly building an extremely heavy building), drilling and injecting liquid into wells, and by coal mining and oil drilling.[28] Perhaps the best known example is the 2008 Sichuan earthquake in China's Sichuan Province in May; this tremor resulted in 69,227 fatalities and is the 19th deadliest earthquake of all time. The Zipingpu Dam is believed to have fluctuated the pressure of the fault 1,650 feet (503 m) away; this pressure probably increased the power of the earthquake and accelerated the rate of movement for the fault.[29] The greatest earthquake in Australia's history is also claimed to be induced by humanity, through coal mining. The city of Newcastle was built over a large sector of coal mining areas. The earthquake has been reported to be spawned from a fault that reactivated due to the millions of tonnes of rock removed in the mining process.[30]
Measuring and locating earthquakes

Main article: Seismology
Earthquakes can be recorded by seismometers up to great distances, because seismic waves travel through the whole Earth's interior. The absolute magnitude of a quake is conventionally reported by numbers on the Moment magnitude scale (formerly Richter scale, magnitude 7 causing serious damage over large areas), whereas the felt magnitude is reported using the modified Mercalli intensity scale (intensity II-XII).
Every tremor produces different types of seismic waves, which travel through rock with different velocities:
Longitudinal P-waves (shock- or pressure waves)
Transverse S-waves (both body waves)
Surface waves—(Rayleigh and Love waves)
Propagation velocity of the seismic waves ranges from approx. 3 km/s up to 13 km/s, depending on the density and elasticity of the medium. In the Earth's interior the shock- or P waves travel much faster than the S waves (approx. relation 1.7 : 1). The differences in travel time from the epicentre to the observatory are a measure of the distance and can be used to image both sources of quakes and structures within the Earth. Also the depth of the hypocenter can be computed roughly.
In solid rock P-waves travel at about 6 to 7 km per second; the velocity increases within the deep mantle to ~13 km/s. The velocity of S-waves ranges from 2–3 km/s in light sediments and 4–5 km/s in the Earth's crust up to 7 km/s in the deep mantle. As a consequence, the first waves of a distant earth quake arrive at an observatory via the Earth's mantle.
Rule of thumb: On the average, the kilometer distance to the earthquake is the number of seconds between the P and S wave times 8.[31] Slight deviations are caused by inhomogeneities of subsurface structure. By such analyses of seismograms the Earth's core was located in 1913 by Beno Gutenberg.
Earthquakes are not only categorized by their magnitude but also by the place where they occur. The world is divided into 754 Flinn-Engdahl regions (F-E regions), which are based on political and geographical boundaries as well as seismic activity. More active zones are divided into smaller F-E regions whereas less active zones belong to larger F-E regions.

مممممممممممممممممشكور اخ محمد
جزاك الله خيرا اخي
وامر اخر أريد ان اوجهه لباقي الاعضاء
أرجو منكم مساعدتنا بالنهوض بالمنتدى
وجلب قدر ممكن من المواضيع والرد على على مواضيع الاخرين ونحن هنا لا لشيء انما لمساعتكم انتم

أنا تحت أمرك وأمر جميع الأعضاء رهن الإشارة ،

جزاكم الله الف خير و يوفق الجميع ان شاء اله مكشورين خوتي

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