نظرات الآخرين لنا هي التي تهدمنا

نظرات الآخرين لنا هي التي تهدمنا

ولو كان كل مَن حولي مِن العُميان ماعدا أنا ..

لما احتجتُ لثيابٍ أنيقة , ولا لمسكنٍ جميل ولا لأثاثٍ فاخر !

لا تكرهوا البلايا الواقعة

قال الحسن البصري:
لا تكرهوا البلايا الواقعة،

والنقمات الحادثة

فلرُبّ أمر تكرهه فيه نجاتك، ولرُبّ أمر تؤثره فيه هلاكك

يُحكَى أنَّ ﺑﺎﺋﻊَ ﺑﺮﺗﻘﺎلٍ اﻧﺘﺼَﺐَ ﻋﻠﻰ ﻗﺎرﻋﺔِ اﻟﻄَّﺮﯾﻖ ﯾﺒﯿﻊُ ﺛﻤﺎرَه، ﻓﻤَﺮَّت ﺑﻘُﺮْبـِهِ ﻋﺠﻮزٌ

 يُحكَى أنَّ ﺑﺎﺋﻊَ ﺑﺮﺗﻘﺎلٍ اﻧﺘﺼَﺐَ ﻋﻠﻰ ﻗﺎرﻋﺔِ اﻟﻄَّﺮﯾﻖ ﯾﺒﯿﻊُ ﺛﻤﺎرَه، ﻓﻤَﺮَّت ﺑﻘُﺮْبـِهِ ﻋﺠﻮزٌ

وﺳﺄلتُه إنْ ﻛﺎﻧﺖ ھﺬه اﻟﺜّﻤﺎر اﻟﻤﻌﺮوﺿﺔ ﻟﻠﺒﯿﻊ ﺣﺎﻣﻀﺔ؟

ظﻦَّ اﻟﺒﺎﺋﻊُ أنّ اﻟﻌﺠﻮزَ ﻻ ﺗﺄﻛﻞُ اﻟﺒﺮﺗﻘﺎلَ اﻟﺤﺎﻣﺾ، ﻓﺮدَّ ﻋﻠﯿﮭﺎ ﻣﺴْﺮِﻋﺎً :

- ﻻ . ھﺬا ﺑﺮﺗﻘﺎلٌ ﺣﻠﻮ. ﻛﻢ ﯾﻠﺰﻣُﻚِ ﯾﺎ ﺳﯿِّﺪَﺗﻲ ؟

- وﻻ ﺣﺒّﺔ واﺣﺪة . أﻧﺎ أرﻏﺐُ ﻓﻲ ﺷﺮاء اﻟﺒﺮﺗﻘﺎل اﻟﺤﺎﻣﺾ، ﻓابنتي ﺣﺎﻣﻞ وھﻲ ﺗﮭْﻮَى أﻛﻞَ ذاك اﻟﺼَّﻨﻒِ ﻣﻦَ اﻟﺒﺮﺗﻘﺎل.

* ھﺎ ﻗﺪْ ﺧﺴِﺮَ اﻟﺒﺎﺋﻊُ اﻟﺼَّﻔﻘﺔ.

بعدَ وﻗﺖٍ طﻮﯾﻞ، اﻗﺘﺮﺑﺖ منه اﻣﺮأةٌ ﺣﺎﻣﻞ، وﺳﺄلَتْه :

- ھﻞ ھﺬا اﻟﺒﺮﺗﻘﺎل ﺣﺎﻣﺾٌ ﯾﺎ ﺳﯿِّﺪي ؟

وﺑﻤﺎ أنّ اﻟﻤﺮأة ﺣﺎﻣﻞ، ﻓﺈن اﻹﺟﺎﺑﺔ ﻛﺎﻧﺖ ﻋﻠﻰ طﺮَفِ ﻟﺴﺎن اﻟﺘّﺎﺟﺮ :

- ﻧﻌﻢ . ھﻮ ﺣﺎﻣﺾٌ ﯾﺎ ﺳﯿِّﺪﺗﻲ. ﻛﻢ ﻛﯿﻠﻮ جرام ﺗـُﺮﯾﺪِﯾﻦ ؟

- ﻟﯿﺴَﺖْ ﻟﻲ رﻏﺒﺔ ﻓﻲ ھﺬا اﻟﺒﺮﺗﻘﺎل، ﻓﺤﻤﺎﺗﻲ ﺗﺤﺒـِّﺬُ اﻟﺒﺮﺗﻘﺎلَ اﻟﺤﻠﻮ، و ﺗﻤْﻘـُﺖُ اﻟﺒﺮﺗﻘﺎلَ اﻟﺤﺎﻣﺾ.

* ھﺎ ھﻮ اﻟﺘّﺎﺟﺮ ﯾﺨﺴَﺮُ ﻣﺮَّةً ﺛﺎﻧﯿﺔً اﻟﺼَّﻔﻘﺔ.

** إنَّ منْ ﯾﺮﯾﺪُ ﺧﺪاعَ اﻵﺧﺮﯾﻦ ﯾﺨْﺪَعُ نفسَهُ ﻗﺒْﻠَﮭُﻢ ~

‏يوافق الاتحاد الأوروبي لكرة القدم (UEFA) على أن الهدف بمجرد انتهاء الازمة

‏يوافق الاتحاد الأوروبي لكرة القدم (UEFA) على أن الهدف بمجرد انتهاء الازمة

سيكون إنهاء مسابقات الأندية والدوريات في اوروبا ، لا حديث عن الغاء ،

‏سيتم تشكيل لجنتين واحده مالية و اخرى لترتيب جداول الدوريات ، و ستُلغى كل مباريات المنتخبات لاعطاء الاندية القدره على مواجهة جداول مضغوطه ،

ايهما افضل المال ام العلم؟؟؟

ايهما افضل المال ام العلم؟؟؟

ذكر في الأثر:ان اهل البصرة اختلفوا

فقال بعضهم:العلم افضل من المال

و قال بعضهم:بل المال افضل من العلم

فأوفدوا رسولا الى بن عباس-رضي الله عنهما-فسأله

فقال ابن عباس : العلم افضل من المال

فقال الرسول : ان سألوني عن الحجة ماذا اقول؟؟؟

قال قل لهم

ان العلم ميراث الانبياء و المال ميراث الفراعنة

ولأن العلم يحرسك و انت تحرس المال

ولأن العلم لا ينقص بالبذل و النفقة, والمال ينقص بالبذل و النفقة

ولأن صاحب المال اذا مات انقطع ذكره, و العالم اذا مات ذكره باق

ولأن صاحب المال ميت وصاحب العلم لا يموت

ولأن صاحب المال يسأل عن كل درهم من اين يكسبه؟و اين انفقه؟

و صاحب العلم له بكل حديث درجة في الجنة

ان كان ولابد من الخيار, فان العلم افضل من المال...ما في ذلك شك

و لكن على ان ينتفع به صاحبه, و ينفع به غيره, فلا يكتمه,ولا يحبسه,

ولا يجعل منه وسيله الى الزلفي,يتزلف به الى ذي جاه او سلطان

ولا يضر به غيره,و لا يخشى في الحق لائما

فلا يداري و لا يداجي, ولا يتأول و يدور حين ينصح او يرشد

ولا يخشى بطش ذي سلطان , و لا بأس ذي بأس

فإذا اتفق لشخص ما العلم و المال, واعطى العلم حقه و المال حقه

و عرف لهما قدرها , و لم يتخذ منهما وسيلة للبطش و البغى

و اعان بماله , و تصدق من فضله فقد ظفر بالحسنين

و نال الأجرين, و ما احسن الدين والدنيا اذا اجتمعا

و صدق رسول الله صلى الله عليه وسلم حينما قال:نعم المال الصالح للرجل الصالح

و قال الإمام علي بن ابي طالب رضي الله عنه

العلم خير من المال, لأن المال تحرسه و العلم يحرسك , و المال تفنيه النفقة و

العلم يزكو على الإنفاق , و العلم حاكم و المال محكوم عليه

مات خزان المال و هم احياء , و العلماء باقون ما بقي الدهر

أعيانهم مفقودة..و آثارهم في القلوب موجودة

Bigg Boss Malayalam

Bigg Boss Malayalam

Bigg Boss (or colloquially Bigg Boss Malayalam) is the Malayalam-language version of Indian reality television series Bigg Boss.[1] It follows the Dutch reality TV series Big Brother which was developed by Endemol in the Netherlands. Bigg Boss was created by Endemol Shine India and telecast on Asianet.[2] The first season was premiered on 24 June 2018 with Mohanlal as the host. The second season premiered on 5 January 2020 with Mohanlal returning as the host.

The show follows selected number of contestants, known as housemates, who are isolated from the outside world for 100 days (or 15 weeks) in a custom built house. The housemates are continuously monitored during their stay in the house by live television cameras as well as personal audio microphones. They are dictated by an omnipresent entity named Bigg Boss. Each week, one or more of the housemates are evicted by a public vote.

Overview

Bigg Boss is a Malayalam-language version of the reality TV franchise Bigg Boss, which is based on the original Dutch Big Brother format developed by John de Mol Jr.. A number of contestants (known as "housemates") live in a purpose-built house and are isolated from the rest of the world. Each week, housemates nominate two of their fellow housemates for eviction, and the housemates who receives the most nominations would face a public vote. Eventually, one housemate would leave after being "evicted" from the House. In the final week, there will be five housemates remaining, and the public will vote for who they wanted to win. Unlike other versions of Big Brother, the Malayalam version uses celebrities as housemates, not members of the general public.

The house is well-furnished and decorated. It has all kinds of modern amenities, but just two bedrooms, living area, kitchen, store room, smoking room, and four toilet bath rooms. There is a garden, pool, activity area and gym in the House. There is also a Confession Room, where the housemates may be called in by Bigg Boss for any kind of conversation, and for the nomination process. The House has no TV connection, no telephones, and no Internet connection.

Rules

They are not supposed to tamper with any of the electronic equipment or any other thing in the House. They aren't allowed to write using paper, book or anything else in the house. They cannot leave the House premises at any time except when they are permitted to. They cannot discuss the nomination process with anyone. They cannot sleep in the day time, are required to wear their mic all the time and speak only in Malayalam.

Sometimes, the housemates may be nominated for other reasons, such as: nomination by a person who has achieved special privileges (via tasks or other things), for breaking rules, or something else. If something very serious happens, a contestant may be evicted immediately. All the rules have never been told to the audience, however, the most prominent ones are clearly seen. The housemates are not permitted to speak in any other language except Malayalam.

Earthquake

Earthquake

An earthquake (also known as a quake, tremor or temblor) is the shaking of the surface of the Earth resulting from a sudden release of energy in the Earth's lithosphere that creates seismic waves. Earthquakes can range in size from those that are so weak that they cannot be felt to those violent enough to propel objects and people into the air, and wreak destruction across entire cities. The seismicity, or seismic activity, of an area is the frequency, type, and size of earthquakes experienced over a period of time. The word tremor is also used for non-earthquake seismic rumbling.

At the Earth's surface, earthquakes manifest themselves by shaking and displacing or disrupting the ground. When the epicenter of a large earthquake is located offshore, the seabed may be displaced sufficiently to cause a tsunami. Earthquakes can also trigger landslides and occasionally, volcanic activity.

In its most general sense, the word earthquake is used to describe any seismic event—whether natural or caused by humans—that generates seismic waves. Earthquakes are caused mostly by rupture of geological faults but also by other events such as volcanic activity, landslides, mine blasts, and nuclear tests. An earthquake's point of initial rupture is called its hypocenter or focus. The epicenter is the point at ground level directly above the hypocenter.

Tectonic earthquakes occur anywhere in the earth where there is sufficient stored elastic strain energy to drive fracture propagation along a fault plane. The sides of a fault move past each other smoothly and aseismically only if there are no irregularities or asperities along the fault surface that increase the frictional resistance. Most fault surfaces do have such asperities, which leads to a form of stick-slip behavior. Once the fault 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.[1] This energy is released as a combination of radiated elastic strain seismic waves,[2] 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.[3]

Earthquake fault types

There are three main types of fault, all of which may cause an interplate 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 where 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.

Reverse faults, particularly those along convergent plate boundaries, are associated with the most powerful earthquakes, megathrust earthquakes, including almost all of those of magnitude 8 or more. Strike-slip faults, particularly continental transforms, can produce major earthquakes up to about magnitude 8. Earthquakes associated with normal faults are generally less than magnitude 7. For every unit increase in magnitude, there is a roughly thirtyfold increase in the energy released. For instance, an earthquake of magnitude 6.0 releases approximately 30 times more energy than a 5.0 magnitude earthquake and a 7.0 magnitude earthquake releases 900 times (30 × 30) more energy than a 5.0 magnitude of earthquake. An 8.6 magnitude earthquake releases the same amount of energy as 10,000 atomic bombs like those used in World War II.[4]

This is so because the energy released in an earthquake, and thus its magnitude, is proportional to the area of the fault that ruptures[5] and the stress drop. Therefore, the longer the length and the wider the width of the faulted area, the larger the resulting magnitude. The topmost, brittle part of the Earth's crust, and the cool slabs of the tectonic plates that are descending down into the hot mantle, are the only parts of our planet that can store elastic energy and release it in fault ruptures. Rocks hotter than about 300 °C (572 °F) flow in response to stress; they do not rupture in earthquakes.[6][7] The maximum observed lengths of ruptures and mapped faults (which may break in a single rupture) are approximately 1,000 km (620 mi). Examples are the earthquakes in Alaska (1957), Chile (1960), and Sumatra (2004), all in subduction zones. The longest earthquake ruptures on strike-slip faults, like the San Andreas Fault (1857, 1906), the North Anatolian Fault in Turkey (1939), and the Denali Fault in Alaska (2002), are about half to one third as long as the lengths along subducting plate margins, and those along normal faults are even shorter.

The most important parameter controlling the maximum earthquake magnitude on a fault, however, is not the maximum available length, but the available width because the latter varies by a factor of 20. Along converging plate margins, the dip angle of the rupture plane is very shallow, typically about 10 degrees.[8] Thus, the width of the plane within the top brittle crust of the Earth can become 50–100 km (31–62 mi) (Japan, 2011; Alaska, 1964), making the most powerful earthquakes possible.

Strike-slip faults tend to be oriented near vertically, resulting in an approximate width of 10 km (6.2 mi) within the brittle crust.[9] Thus, earthquakes with magnitudes much larger than 8 are not possible. Maximum magnitudes along many normal faults are even more limited because many of them are located along spreading centers, as in Iceland, where the thickness of the brittle layer is only about six kilometres (3.7 mi).[10][11]

In addition, there exists a hierarchy of stress level in the three fault types. Thrust faults are generated by the highest, strike-slip by intermediate, and normal faults by the lowest stress levels.[12] This can easily be understood by considering the direction of the greatest principal stress, the direction of the force that "pushes" the rock mass during the faulting. In the case of normal faults, the rock mass is pushed down in a vertical direction, thus the pushing force (greatest principal stress) equals the weight of the rock mass itself. In the case of thrusting, the rock mass "escapes" in the direction of the least principal stress, namely upward, lifting the rock mass up, and thus, the overburden equals the least principal stress. Strike-slip faulting is intermediate between the other two types described above. This difference in stress regime in the three faulting environments can contribute to differences in stress drop during faulting, which contributes to differences in the radiated energy, regardless of fault dimensions.

Earthquakes away from plate boundaries

Where plate boundaries occur within the 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.[13]

All tectonic plates have internal stress fields caused by their interactions with neighboring plates and sedimentary loading or unloading (e.g., deglaciation).[14] These stresses may be sufficient to cause failure along existing fault planes, giving rise to intraplate earthquakes.[15]

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 (43 mi) are classified as "shallow-focus" earthquakes, while those with a focal-depth between 70 and 300 km (43 and 186 mi) 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 to 700 km (190 to 430 mi)).[16] 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.[17]

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 1980 eruption of Mount St. Helens.[18] 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.[19]

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 (330 ft) 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.[20]

Rupture propagation is generally modeled 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, which 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 neighboring coast, as in the 1896 Sanriku earthquake.[20]

Tidal forces

Tides may induce some seismicity. See tidal triggering of earthquakes for details.

Earthquake clusters

Most earthquakes form part of a sequence, related to each other in terms of location and time.[21] 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.[22]

Aftershocks

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.[21]

Earthquake swarms

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, so none has a notable higher magnitude than another. An example of an earthquake swarm is the 2004 activity at Yellowstone National Park.[23] In August 2012, a swarm of earthquakes shook Southern California's Imperial Valley, showing the most recorded activity in the area since the 1970s.[24]

Sometimes a series of earthquakes occur in what has been called an 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.[25][26]

Intensity of earth quaking and magnitude of earthquakes

Quaking or shaking of the earth is a common phenomenon undoubtedly known to humans from earliest times. Prior to the development of strong-motion accelerometers that can measure peak ground speed and acceleration directly, the intensity of the earth-shaking was estimated on the basis of the observed effects, as categorized on various seismic intensity scales. Only in the last century has the source of such shaking been identified as ruptures in the Earth's crust, with the intensity of shaking at any locality dependent not only on the local ground conditions but also on the strength or magnitude of the rupture, and on its distance.[27]

The first scale for measuring earthquake magnitudes was developed by Charles F. Richter in 1935. Subsequent scales (see seismic magnitude scales) have retained a key feature, where each unit represents a ten-fold difference in the amplitude of the ground shaking and a 32-fold difference in energy. Subsequent scales are also adjusted to have approximately the same numeric value within the limits of the scale.[28]

Although the mass media commonly reports earthquake magnitudes as "Richter magnitude" or "Richter scale", standard practice by most seismological authorities is to express an earthquake's strength on the moment magnitude scale, which is based on the actual energy released by an earthquake.[29]

Frequency of occurrence

It is estimated that around 500,000 earthquakes occur each year, detectable with current instrumentation. About 100,000 of these can be felt.[30][31] Minor earthquakes occur nearly constantly around the world in places like California and Alaska in the U.S., as well as in El Salvador, Mexico, Guatemala, Chile, Peru, Indonesia, Philippines, Iran, Pakistan, the Azores in Portugal, Turkey, New Zealand, Greece, Italy, India, Nepal and Japan.[32] 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.[33] 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.[34] This is an example of the Gutenberg–Richter law.