A master equation for gravitational perturbations of maximally symmetric black holes in hig

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双星轨道半径与质量的关系推导

双星轨道半径与质量的关系推导

双星轨道半径与质量的关系推导The relationship between the orbital radius and mass of a binary star system can be derived using the laws of celestial mechanics. According to Newton's law of universal gravitation, the gravitational force between two objects is directly proportional to the product of their masses and inversely proportional to the square of their distance apart.In a binary star system, considering two stars with masses m1 and m2 respectively, revolving around their center of mass, we can derive an equation for the gravitational force acting on each star. Let r be the distance between the centers of mass of the two stars, and let R be the distance from either star to the center of mass.根据双星轨道半径和质量之间的关系,可以使用天体力学定律进行推导。

根据牛顿的普适引力定律,两个物体之间的引力与它们的质量乘积成正比,与它们的距离平方成反比。

在一个双星系统中,考虑到两颗质量分别为m1和m2的恒星围绕它们质心旋转,我们可以推导出作用在每颗恒星上的引力方程。

牛顿万有引力的作文素材

牛顿万有引力的作文素材

牛顿万有引力的作文素材英文回答:Newton's law of universal gravitation states that every particle in the universe attracts every other particle with a force that is directly proportional to the product of their masses and inversely proportional to the square of the distance between their centers. This force is known as gravitational force.Gravitational force plays a crucial role in the dynamics of our universe. It governs the motion ofcelestial bodies, such as planets, moons, and stars. For example, the gravitational force between the Earth and the Moon keeps the Moon in orbit around the Earth. Similarly, the gravitational force between the Sun and the planets keeps them in their respective orbits.The law of universal gravitation can be expressed mathematically as F = G (m1 m2) / r^2, where F is thegravitational force, G is the gravitational constant, m1 and m2 are the masses of the two objects, and r is the distance between their centers. The gravitational constant, G, is approximately equal to 6.67430 × 10^-11 N(m/kg)^2.The law of universal gravitation is a fundamental principle in physics and has been verified by numerous experiments and observations. It explains why objects fall to the ground when dropped and why planets orbit around the Sun. It also provides a basis for understanding the motion of objects in space and the formation of galaxies.中文回答:牛顿的万有引力定律表明,宇宙中的每个粒子都会以与其质量乘积成正比、与他们之间距离的平方成反比的力吸引彼此。

星体之间的重力势能

星体之间的重力势能

星体之间的重力势能The gravitational potential energy between celestial bodies is a fundamental concept in physics that plays a crucial role in understanding the dynamics of the universe. This potential energy arises due to the attractive force of gravity between two or more objects, such as stars, planets, or moons. In this discussion, we will explore the conceptof gravitational potential energy from various perspectives, including its definition, formula, and its significance in astrophysics and cosmology.Gravitational potential energy can be defined as the energy possessed by an object or a system of objects due to their positions in a gravitational field. It is directly related to the mass of the objects and the distance between them. The greater the mass of the objects and the closer they are, the higher the gravitational potential energy. This potential energy is a scalar quantity, meaning it only has magnitude and no direction.The formula to calculate the gravitational potential energy between two objects is given by the equation:PE = -G * (m1 * m2) / rWhere PE represents the gravitational potential energy, G is the gravitational constant (approximately 6.67430 × 10^-11 N m^2/kg^2), m1 and m2 are the masses of the two objects, and r is the distance between their centers of mass.From an astrophysical perspective, the concept of gravitational potential energy is crucial in understanding the formation and evolution of celestial bodies. During the formation of stars, for example, gravitational potential energy plays a significant role in the collapse of interstellar gas and dust clouds, leading to the formation of protostars. As the protostar continues to accrete mass, the gravitational potential energy increases, and this energy is eventually converted into thermal energy, powering the star's nuclear fusion processes.In cosmology, gravitational potential energy is also important in understanding the large-scale structure of the universe. The distribution of matter and energy in the universe is influenced by the gravitational potentialenergy between galaxies, galaxy clusters, and even larger cosmic structures. The gravitational potential energy acts as a driving force for the formation of cosmic filaments, voids, and superclusters, shaping the overall structure of the universe.Moreover, gravitational potential energy is intimately connected to the concept of escape velocity. Escapevelocity is the minimum velocity an object needs to escape the gravitational pull of a celestial body. It is directly related to the gravitational potential energy of the object. By calculating the escape velocity, scientists candetermine whether an object, such as a spacecraft or a planet, can overcome the gravitational pull and leave the vicinity of a celestial body.Furthermore, the concept of gravitational potential energy is closely related to the principle of conservationof energy. In a closed system, the total energy, including the gravitational potential energy, remains constant. This principle allows scientists to study the interplay between different forms of energy, such as kinetic energy and gravitational potential energy, in various astrophysical phenomena.In conclusion, the gravitational potential energy between celestial bodies is a fundamental concept in physics that has wide-ranging implications in astrophysics and cosmology. It is defined as the energy possessed by objects due to their positions in a gravitational field and can be calculated using the gravitational potential energy formula. This concept is crucial in understanding the formation and evolution of celestial bodies, the large-scale structure of the universe, escape velocity, and the conservation of energy. By studying gravitational potential energy, scientists can gain valuable insights into the dynamics and behavior of the universe at both small and large scales.。

牛顿万有引力定律的英语

牛顿万有引力定律的英语

牛顿万有引力定律的英语In the realm of physics, Sir Isaac Newton's law of universal gravitation stands as a cornerstone of understanding the forces that govern celestial bodies. It elegantly explains how every object in the universe attracts every other object with a force that is proportional to the product of their masses and inversely proportional to the square of the distance between their centers.This fundamental principle, first articulated in the late 17th century, has withstood the test of time, shaping our comprehension of how planets orbit the sun, how moons orbit planets, and even how tides are influenced by the gravitational pull of the moon and the sun.Newton's law of universal gravitation is encapsulated in the equation \( F = G \frac{m_1 m_2}{r^2} \), where \( F \) is the force of attraction, \( G \) is the gravitational constant, \( m_1 \) and \( m_2 \) are the masses of the two objects, and \( r \) is the distance between their centers. It's a formula that has guided countless scientific endeavors and space missions.Despite its simplicity, the implications of this law are profound. It has been instrumental in the development of modern astronomy and has been a key factor in the design of spacecraft trajectories, ensuring that they can navigate the vast distances of space with precision.As we delve deeper into the cosmos, the law of universal gravitation remains a vital tool in our scientific arsenal. It is a testament to Newton's genius and the enduring legacy of his work, which continues to inspire new generations of scientists and thinkers to explore the mysteries of the universe.。

宇宙空间公式大全

宇宙空间公式大全

宇宙空间公式大全宇宙空间是兴趣和研究的中心,人类对它的认知和探索不断深入。

导致此认知和探索的背后是众多的公式和理论。

本文将向您介绍一些与宇宙空间相关的重要公式和理论,希望对您的学习和研究提供一些参考。

1. 牛顿第二定律(Newton's Second Law)F = ma这是牛顿的经典力学定律之一,它描述了物体的加速度与作用于其上的力的关系,其中F代表力,m代表物体的质量,a代表物体的加速度。

2. 万有引力定律(Universal Law of Gravitation)F=G*(m1*m2/r^2)这是牛顿力学理论的另一项重要成果,描述了两个物体之间的引力关系,其中F代表引力,G代表引力常数,m1和m2分别代表两个物体的质量,r代表两个物体之间的距离。

3. 爱因斯坦相对论(Einstein's Theory of Relativity)E = mc^2这是阐明了质能等价性的公式,其中E代表能量,m代表物体的质量,c代表光速。

4. 扩张宇宙理论(Theory of Cosmic Expansion)Hubble定律:v = H0 * d它描述了宇宙中的星系相对于地球的运动速度与它们之间的距离的关系,其中v代表星系相对于地球的速度,H0代表哈勃常数,d代表星系相对于地球的距离。

5. 热辐射光谱(Blackbody Radiation Spectrum)Eλ = (8πhc / λ^5) * (1 / (exp(hc / (λkt)) - 1))它描述了一个黑体辐射的光谱能量密度,其中Eλ代表单位波长范围内的光能量密度,h代表普朗克常数,c代表光速,λ代表波长,k代表玻尔兹曼常数,t代表温度。

6. 热力学中的熵(Entropy in Thermodynamics)ΔS=Q/T这个公式描述了一个封闭系统的熵变化,其中ΔS代表熵变,Q代表系统吸收或释放的热量能量,T代表系统的温度。

7. 薛定谔方程(Schrodinger Equation)iħ∂Ψ/∂t=ĤΨ这是量子力学中描述波函数演化的方程,其中i代表虚数单位,ħ代表约化普朗克常数,Ψ代表波函数,t代表时间,Ĥ代表系统哈密顿算符。

高一必修一物理公式大全总结

高一必修一物理公式大全总结

高一必修一物理公式大全总结Physics is a fascinating subject that allows us to understand the fundamental principles that govern the universe. As high school students in the first year, it is crucial to grasp the essential physics formulas to succeed in the course. These formulas serve as the building blocks for more complex concepts and calculations in the future.物理是一门令人着迷的学科,它让我们能够理解控制宇宙的基本原理。

作为高一学生,掌握基本的物理公式对于在课程中取得成功至关重要。

这些公式为未来更复杂的概念和计算奠定了基础。

One of the most important formulas in physics is Newton's second law, which states that the force acting on an object is equal to the mass of the object multiplied by its acceleration. This formula, F = ma, is fundamental to understanding how objects move and interact with each other in the physical world.物理学中最重要的公式之一是牛顿第二定律,它规定作用于物体上的力等于物体的质量乘以它的加速度。

这个公式 F = ma 是理解物体如何在物理世界中移动和相互作用的基础。

爱因斯坦的英文介绍

爱因斯坦的英文介绍
In 1952, Einstein was offered the presidency of Israel, which he declined, stating that he lacked the necessary people skills for the job. Einstein's health declined in the following years, and he passed away on April 18, 1955, leaving behind a legacy that continues to inspire and influence scientists and thinkers around the world. His contributions to science and society have left an indelible mark on the human quest for knowledge and understanding of the universe, making him one of the most celebrated and revered figures in history.
After the war, Einstein became an advocate for nuclear disarmament and a supporter of the civil rights movement in the United States. He was an outspoken critic of McCarthyism and an active proponent of world government and democratic socialism. He also continued to work on a unified field theory, seeking to unify the forces of electromagnetism and gravity into a single framework, though he was unable to achieve this goal by the end of his life.

港航专业英语

港航专业英语

23Scott L.DouglassRobert A.NathanJeffrey D.MalyszekProfessorDepartment of Civil Engineering University of South AlabamaMobile,AlabamaMoffat &Nichol EngineersTampa,FloridaMoffat &Nichol EngineersTampa,FloridaC OASTAL AND P ORTE NGINEERINGCoastal and port engineering encom-passes planning,design,and construc-tion of projects to satisfy society’s needs and concerns in the coastal environ-ment,such as harbor and marina development,shore protection,beach nourishment,and other constructed systems in the coastal wave and tide environment.Over time,the scope of this field of engineering has broadened from only navigation improvement and property protection to include recreational beaches and environmental considerations.It takes into account the environmental conditions unique to the coastal area,including wind,waves,tides,and sand movement.Thus,coastal engineering makes extensive use of the sciences of oceanogra-phy and coastal geomorphology as well as of geo-technical,environmental,structural,and hydraulic engineering principles.23.1Risk Level in Coastal ProjectsBecause of the nature of littoral drift,or longshore sand transport along the coasts,erosion caused by coastal engineering projects along adjacent shore-lines,sometimes several miles away,has been a recurring problem.Tools for prediction and evaluation of such shoreline dynamics are con-tinually improving but are still limited,in partbecause of nature’s unpredictability.Hence,post-construction monitoring of the response of nearby beaches is often a required component of coastal engineering projects.The design level of risk in many coastal engi-neering projects may be higher than in other civil engineering disciplines because the price of more effective design is often not warranted.The design environment is very challenging.It varies with time,since design conditions are often affected by storms that contain much more energy and induce very different loadings from those normally experienced.Also,because the physical processes are so complex,often too complex for theoretical description,the practice of coastal engineering is still much of an art.Con-sequently,practitioners should have a broad base of practical experience and should exercise sound judgment.The practice of coastal engineering has changed rapidly in the last several decades owing to in-creases in natural pressures,such as that created by sea-level rise,and societal pressures,such as those from growing populations along the coast with greater environmental awareness.The changes are recorded in the proceedings of specialty confer-ences,such as those of the American Society of Civil Engineering (ASCE),including Coastal Engineering Practice;Dredging,Ports,Coastal Sedi-ments,Coastal Zone,International Coastal Engin-eering Conference,and the Florida Shore andSource: Standard Handbook for Civil EngineersBeach Preservation Association’s Beach preser-vation Technology Conference series.Coastal Hydraulics and SedimentsWaves often apply the primary hydraulic forces of interest in coastal engineering.Tides and other water-level fluctuations control the location of wave attack on the shoreline.Waves and tides generate currents in the coastal zone.Breaking waves provide the forces that drive sand transport along the coast and can cause beach changes,including erosion due to coastal engineering projects.23.2Characteristics of WavesWater waves are caused by a disturbance of the water surface.The original disturbance may be caused by wind,boats or ships,earthquakes,or the gravitational attraction of the moon and sun.Most of the waves are initially formed by wind.Waves formed by moving ships or boats are wakes .Waves formed by earthquake disturbances are tsunamis .Waves formed by the gravitational attraction of the moon and sun are tides .After waves are formed,they can propagate across the surface of the sea for thousands of miles.The properties of propagating waves have been the subject of various wave theories for over a century.The most useful wave theory for engineers is the linear,or small-amplitude,theory.23.2.1Linear Wave TheoryEssentially,linear wave theory treats only a train of waves of the same length and period in a constant depth of water.As in optics,this is called a monochromatic wave train.Linear wave theory relates the length,period,and depth of waves as indicated by Eq.(23.1).L ¼gT 22p tan h 2p dL(23:1)where L ¼wavelength,ft,the horizontal distancebetween crestsd ¼vertical distance,ft,between mean orstill water level and the bottom g ¼acceleration due to gravity,32.2ft /s T ¼wave periods,the time required forpropagation of a wave crest over the wavelength (Fig.23.1)Wave height H ,the fourth value needed to com-pletely define a monochromatic wave train,is an independent value in linear wave theory,but not for higher-order wave theories (Art.23.2.2).Fig.23.1Wave in shallow water.Water particles follow an elliptical path.L indicates length of wave,crest to crest;H wave height,d depth from still-water level to the bottom.The wave period T is the time for a wave to move the distance L .23.2n Section Twenty-ThreeEquation (23.1),implicit in terms of L ,requires an iterative solution except for deep or shallow water.When the relative depth d /L is greater than 1⁄2,the wave is in deep water and Eq.(23.1)becomesL ¼gT 22(23:2)For shallow water,d =L ,1⁄25,eq.(23.1)reduces toL ¼T ffiffiffiffiffigd p (23:3)Individual water particles follow a closed orbit.They return to the same location with each passing wave.The orbits are circular in deep water and elliptical in shallow water.Linear wave theory equations for the water-particle trajectories,the fluctuating water-particle velocities and accelera-tions,and pressures under wave trains are given in R.G.Dean and R.A.Dalrymple,“Water Wave Mechanics for Scientists and Engineers,”Prentice-Hall,Englewood Cliffs,N.J.();R.M.Sorenson,“Basic Wave Mechanics:For Coastal and Ocean Engineers,”John Wiley &Sons,Inc.,New York ().)23.2.2Higher-Order Wave TheoriesThe linear wave theory provides adequate approxi-mations of the kinematics and dynamics of wave motion for many engineering applications.Some areas of concern to civil engineers where the linear theory is not adequate,however,are very large waves and shallow water.Higher-order wavetheories,such as Stokes’second order and cnoidal wave theories,address these important situations.Numerical wave theories,however,have the broadest range of eful tables from stream-function wave theory,a higher-order,num-erical theory,are given in R.G.Dean,“Evaluation and Development of Water Wave Theories For Engineering Applications,”Special Report No.1,U.S.Army Coastal Engineering Research Center,Ft.Belvoir,Va.Determination of the water surface elevations for large waves or waves in shallow water requires use of a higher-order wave theory.A typical waveform is shown in Fig.23.2.The crest of the wave is more peaked and the trough of the wave is flatter than for the sinusoidal water surface profile in linear wave theory.For a horizontal bottom,the height of the wave crest above the still-water level is a maximum of about 0.8d .(“Shore Protection Manual,”4th ed.,U.S.Army Coastal Engineering Research Center,Government Printing Office,Washington,D.C.();“Coastal Engineering Manual,”( /inet /usace-docs /eng-manuals /em-htm).)23.2.3Wave TransformationsAs waves move toward the coast into varying water depths,the wave period remains constant (until breaking).The wavelength and height,how-ever,change because of shoaling,refraction,diffraction,reflection,and wavebreaking.Fig.23.2Water surface for a large wave in shallow water.Coastal and Port Engineering n 23.3Shoaling n As a wave moves into shallower water the wavelength decreases,as indicated by Eq.(23.1),and the wave height increases.The increase in wave height is given by the shoaling coefficient K s.K s¼HH0o(23:4)where H¼wave height in a specific depth of water H0o¼deep-water unrefracted wave height K s varies as a function of relative depth d/L as shown in Table23.1.For an incident wave train of period T,Table23.1can be used to estimate the wave height and wavelength in any depth with Eq.(23.2)for L o.Refraction n This is a term,borrowed from optics,for the bending of waves as they slow down. As waves approach a beach at an angle,a portion of the wave is in shallower water and moving more slowly than the rest.Viewed from above,the wave crest appears to bend.Refraction changes the height of waves as well as the direction of propagation.Refraction can cause wave energy to be focused on headlands and defocused from embayments.There are two general types of refraction models.Wave-ray models trace the path of wave rays,lines perpendicular to the wave crests.The other type of computer refraction model computes solutions to differential equations for the wave-heightfield.The physics simulated varies slightly from model to model.Diffraction n Another term borrowed from optics,this is the spread of energy along a wave crest.An engineering example of wave diffraction is the spreading of energy around the tip of a breakwater into the lee of the breakwater.The wave crest wraps around the tip of a breakwater and appears to be propagating away from that point.Diffraction also occurs in open water where refraction occurs.It can reduce the focusing and bending due to refraction.Reflection n Waves are reflected from obstruc-tions in their path.Reflection of wave energy is greatest at vertical walls,90%to100%,and least for beaches and rubble structures.Undesirable wave-energy conditions in vertical-walled marinas can often be reduced by placing rubble at the water line.Breaking n This happens constantly along a beach,but the mechanics are not well modeled by theory.Thus,much of our knowledge of breaking is empirical.In shallow water,waves break when they reach a limiting depth for the individual wave. This depth-limited breaking is very useful in coastal structure design and surf-zone dynamics models.For an individual wave,the limiting depth is about equal to the water depth and lies in the range given by Eq.(23.5.).0:8,Hdmax,1:2(23:5)where(H/d)max¼maximum ratio of wave height to depth below mean water level for a breaking wave.The variation in(H/d)b(the subscript b means breaking)is due to beach slope and wave steepness H/L.Equation(23.5)is often useful in selecting the design wave height for coastal structures in shal-low water.Given an estimate of the design water depth at the structure location,the maximum wave height H max that can exist in that depth of water is about equal to the depth.Any larger waves would have already broken farther offshore and been reduced to H max.23.2.4Irregular WavesThe smooth water surfaces of monochromatic wave theories are not realistic representations ofTable23.1Shoaling Coefficient and Wavelength Changes as Waves Move into Shallower Waterd/L o d/L K s0.0050.028 1.700.0100.040 1.430.0200.058 1.230.0300.071 1.130.0400.083 1.060.0500.094 1.020.100.140.200.220.300.310.500.50 1.023.4n Section Twenty-Threethe real surf zone.Particularly under an active wind,the water surface will be much more irregular.Two different sets of tools have been developed by oceanographers to describe realistic sea surfaces.One is a statistical representation and one is a spectral representation.Statistics of Wave Height n The individual waves in a typical sea differ in height.The heights follow a theoretical Rayleigh distribution in deep water.In shallow water,the larger individual waves break sooner,and thus the upper tail of the distribution is lost.A commonly used,single wave-height para-meter is the significant wave height H1/3.This is the average of the highest one-third of the waves. Other wave heights used in design can be related to H1/3via the Rayleigh distribution as indicated in Table23.2.23.2.5Wave SpectraSpectral techniques are available that describe the amount of energy at the different frequencies or wave periods in an irregular sea.They provide more information about the irregular wave train and are used in some of the more advanced coastal-structure design methods.A wave-height parameter that is related to the total energy in asea is H mo .(H mois often called significant waveheight also.)Significant wave height H s is a term that has a long history of use in coastal engineering and oceanography.As indicated above and in Art.23.2.4,two fundamentally different definitions for significant wave height are used in coastal engineering.One is statistically based and the other is energy-or spectral-based.Since they are different,the notations,H1/3and H moare recom-mended to avoid confusion in use of H s:H1=3¼statistical significant wave heightH mo¼spectral significant wave heightIn deep water,H mois approximately equal to H1/3. In shallow water,and in particular in the surf zone, the two parameters diverge.(There is little that is truly significant about either parameter.Few of the waves in an actual wave train will have the significant height.It is basically a statistical artifact.)Transformations of actual wave seas such as shoaling,refraction,diffraction,and breaking are not completely understood and not well modeled. Although the monochromatic wave transforma-tions are well modeled,as described in the preceding,in actuality the individual waves and wave trains interact with each other and change the wavefield.(These wave-wave interactions are the subject of significant research efforts.)Thus, the more realistic conditions,that is,irregular seas, are the least understood.However,models that account for the transformation of wave spectra across arbitrary bottom contours are available.23.2.6Wave Generation by Wind Waves under the influence of the winds that generated them are called sea.Waves that have propagated beyond the initial winds that generated them are called swell.Fetch is the distance that a wind blows across the water.For enclosed bays,this is the distance across the water body in the direction of the wind. Duration is the time that a wind at a specific speed blows across the water.The waves at any spot may be fetch-limited or duration-limited.When a windTable23.2Wave Heights Used in DesignSymbol Description Multiple of H1/3 H1/3Average height of highest one-third of waves 1.0H av Average wave height0.6H10Average height of highest10%of waves 1.3H1%Wave height exceeded1%of the time 1.6H sin Height of simple sine waves with same energyas the actual irregular height wave train 0.8Coastal and Port Engineering n23.5starts to blow,wave heights are limited by the short time that the wind has blown;in other words,they are duration-limited.Seas not duration-limited are fully arisen .If the waves are limited by the fetch,they are fetch-limited.For enclosed bay and lake locations,simple parametric models can provide useful wave information.Table 23.3gives wave height and wave period estimates for deep water for different fetch distances and different wind speeds.The values are based on the assumption that the wind blows for a sufficient time to generate fully arisen conditions.In shallow water,the wave heights will be less.On the open ocean,waves are almost never fetch-limited.They are free to continue to move after the wind ceases or changes.Swell wave energy can propagate across entire oceans.The waves striking the beach at any moment in time may include swell from several different locations plus a local wind sea.Thus,for an open-ocean situation,numerical models that grid the entire ocean are required to keep track of wave-energy propagation and local generation.Wave-generation models can forecast waves for marine construction operations.They can also hindcast,that is,estimate waves based on measured or estimated winds at times in the past,for wave climatology studies,probabilistic design,or historic performance analysis.The U.S.Army Corps of Engineers “Wave Information Study(WIS)”has hindcast 40years of data,1956–1995,to generate probabilistic wave statistics for hun-dreds of locations along the coasts of the United States.The wave statistics are available in tabular form,and the actual time sequence of wave conditions is available in digital form.(J.B.Herbich,“Handbook of Coastal and Ocean Engineering,”Gulf Publishing Company,Houston,Tex ().)23.2.7Ship and Boat WakesShip wakes are sometimes the largest waves that occur at a location and thus become the design wave.Vessel wakes from large ships can be up to 6ft high and have wave periods less than 3s.Ship wakes can be estimated with methods presented in J.R.Weggel and R.M.Sorensen,“Ship Wave Prediction for Port and Channel Design,”Proceed-ings,Port Conference,1986,ASCE.Approaches for estimating the wakes due to recreational boats are presented in ASCE Manual 50,“Planning and Design Guidelines for Small-Craft Harbors,”and R.R.Bottin et al.,“Maryland Guide Book for Marina Owners and Operators on Alternatives Available for the Protection of Small Craft against Vessel Generated Waves,”U.S.Army Corps of Engineers Coastal Engineering Research Center,Washington,D.C.Table 23.3Spectral Significant Heights and Periods for Wind-Generated Deep-Water Waves*Wind speed,knotsFetch length,statute miles0.512105020H m o ,ft 0.60.8 1.1 2.2 4.1T p ,s 1.3 1.6 2.0 3.2 4.740H m o ,ft 1.3 1.8 2.5 5.411T p ,s 1.7 2.2 2.7 4.5760H m o ,ft 2.2 3.1 4.29.118T p ,s2.12.63.25.48*Based on method presented in S.L.Douglass et al.,“Wave Forecasting for Construction in Mobile Bay,”Proceedings,Coastal Engineering Practice,1992,pp.713–727,American Society of Civil Engineers.H m o ¼spectral significant wave height and T p ¼wave period.23.6n Section Twenty-Three23.3Design Coastal WaterLevelsThe design water level depends on the type of project.For design of some protective coastal structures,for example,a water level based on a recurrence interval such as a10-year or100-year return period often is selected.The Federal Emergency Management Agency(FEMA)“Flood Insurance Rate Maps(FIRM)”are based on such a concept.They provide afirst estimate of high-water levels along the U.S.coastlines.Since the design of some coastal structures can be extremely sensitive to the design water level,more in-depth analysis may be justified.For engineering projects con-cerned with normal water levels,for example, where dock elevations and beachfill elevations are determined by the water level,an estimate of the normal water level and the normal range around that mean is needed.All coastal engineer-ing projects should be designed to take into account the full range of potential water levels.The water level at any time in a specific location is influenced by the tides,mean sea-level elevation, storm surge,including wind influence,and other local influences,such as fresh-water inflow in estuaries.Tides n The tide is the periodic rise and fall of ocean waters produced by the attraction of the moon and sun.Generally,the average interval between successive high tides is12h25min,half the time between successive passages of the moon across a given meridian.The moon exerts a greater influence on the tides than the sun.Tides,however, are often affected by meteorological conditions, including propagation of storm tides from the sea into coastal waters.The highest tides,which occur at intervals of half a lunar month,are called spring tides.They occur at or near the time when the moon is new or full,i.e.,when the sun,moon,and earth fall in line, and the tide-generating forces of the moon and sun are additive.When the lines connecting the earth with the sun and the moon form a right angle,i.e., when the moon is in its quarters,then the actions of the moon and sun are subtractive,and the lowest tides of the month,the neap tides,occur.Tidal waves are retarded by frictional forces as the earth revolves daily around its axis,and the tide tends to follow the direction of the moon.Thus,the highest tide for each location is not coincident with conjunction and opposition but occurs at some constant time after new and full moon.This interval,known as the age of the tide,may amount to as much as21⁄2days.Large differences in tidal range occur at different locations along the ocean coast.They arise because of secondary tidal waves set up by the primary tidal wave or mass of water moving around the earth.These movements are also in-fluenced by the depth of shoaling water and con-figuration of the coast.The highest tides in the world occur in the Bay of Fundy,where a rise of 100ft has been recorded.Inland and landlocked seas,such as the Mediterranean and the Baltic, have less than1ft of tide,and the Great Lakes are not noticeably influenced.Tides that occur twice each lunar day are called semidiurnal tides.Since the lunar day,or time it takes the moon to make a complete revolution around the earth,is about50min longer than the solar day,the corresponding high tide on succes-sive days is about50min later.In some places,such as Pensacola,Florida,only one high tide a day occurs.These tides are called diurnal tides.If one of the two daily high tides is incomplete,i.e.,if it does not reach the height of the previous tide,as at San Francisco,then the tides are referred to as mixed diurnal tides.Table23.4gives the spring and mean tidal ranges for some major ports.There are other exceptional tidal phenomena. For instance,at Southampton,England,there are four daily high waters,occurring in pairs,separa-ted by a short interval.At Portsmouth,there are two sets of three tidal peaks per day.Tidal bores,a regular occurrence at certain locations are high-crested waves caused by the rush offlood tide up a river,as in the Amazon,or by the meeting of tides, as in the Bay of Fundy.The rise of the tide is referred to some estab-lished datum of the charts,which varies in different parts of the world.In the United States,it is mean lower low water(MLLW).Mean high water is the average of the high water over a19-year period,and mean low water is the average of the low water over a19-year period. Higher high water is the higher of the two high waters of any diurnal tidal day,and lower low water is the lower of the two low waters of any diurnal tidal day.Mean higher high water is the average height of the higher high water over a19-year period,and mean lower low water is the Coastal and Port Engineering n23.7average height of the lower low waters over a 19-year period (tidal epoch).Highest high water and lowest low water are the highest and lowest,respectively,of the spring tides of record.Mean range is the height of mean high water above mean low water.The mean of this height is generally referred to as mean sea level (MSL).Diurnal range is the difference in height between the mean higher high water and the mean lower low water.The National Ocean Service annually publishes tide tables that give the time and elevation of the high and low tides at thousands of locations around the world and that can be used to forecast water levels at all times.The tide tables forecast the repeating,astronomical portions of the tide for specific locations but do not directly account for the day-to-day effects of changes in local winds,pressures,and other factors.Along most coasts,the tide table forecasts are within 1ft of the actual water level 90%of the time.Relative sea-level rise is gradually changing all of the epoch-based datum at any coastal site.Although,the datum that is used for design and construction throughout an upland area is not particularly important,the relation between con-struction and actual water levels in the coastal zone can be extremely important.The level of the oceans of the world has been gradually increasing for thousands of years.The important change is the relative sea-level change,the combined effect of water level and land-mass elevation changes due to subsidence (typical of the U.S.Atlantic and Gulf coasts)or rebound or emergence (Pacific coast of the U.S.).Measured,long-term tide data for major U.S.ports show that the relative sea-level rise differs from location to location.For example,Table 23.4Mean and Spring Tidal Ranges for Some of the World’s Major Ports*Mean range,ftSpring range,ft Anchorage,Alaska 26.729.6†Antwerp,Belgium15.717.8Auckland,New Zealand 8.09.2Baltimore,Md 1.1 1.3Bilboa,Spain 9.011.8Bombay,India 8.711.8Boston,Mass.9.511.0Buenos Aires,Argentina2.2 2.4Burntcoat Head,Nova Scotia (Bay of Fundy)41.647.5Canal Zone,Atlantic side 0.7 1.1†Canal Zone,Pacific side 12.616.4Capetown,Union of South Africa 3.8 5.2Cherbourg,France 13.018.0Dakar,Africa 3.3 4.4Dover,England 14.518.6Galveston,Tex 1.0 1.4†Genoa,Italy 0.60.8Gibraltar,Spain2.33.1Hamburg,Germany 7.68.1Havana,Cuba1.0 1.2Hong Kong,China 3.1 5.3†Honolulu,Hawaii 1.2 1.9†Juneau,Alaska14.016.6†La Guaira,Venezuela 1.0†Lisbon,Portugal 8.410.8Liverpool,England 21.227.1Manila,Philippines 3.3†Marseilles,France 0.40.6Melbourne,Australia 1.7 1.9Murmansk,U.S.S.R.7.99.9New York,N.Y. 4.4 5.3Osaka,Japan 2.5 3.3Oslo,Norway 1.0 1.1Quebec,Canada 13.715.5Rangoon,Burma 13.417.0Reikjavik,Iceland 9.212.5Rio de Janeiro,Brazil 2.5 3.5Rotterdam,Netherlands 5.0 5.4San Diego,Calif. 4.2 5.8†San Francisco,Calif. 4.0 5.7†San Juan,Puerto Rico 1.1 1.3Seattle,Wash.7.611.3†Shanghai,China 6.78.9Singapore,Malaya5.67.4Table 23.4(Continued )Mean range,ftSpring range,ft Southampton,England 10.013.6Sydney,Australia 3.6 4.5Valparaiso,Chile 3.0 3.9Vladivostok,U.S.S.R.0.60.7Yokohama,Japan 3.5 4.7Zanzibar,Africa8.812.4*“Tide Tables,”National Ocean Service.†Diurnal range.23.8n Section Twenty-Threeat Galveston,Tex.,there has been about1ft of relative sea-level rise during the last50years.At Anchorage,Alaska,there has been about2ft of relative sea-level fall during the last50years.The impact of long-term sea-level rise has rarely been taken into account in design,except when it has already impacted the epoch-based tidal datum, such as MLLW.The National Geodetic Vertical Datum(NGVD)was established at the mean sea level(MSL)of1929.Since sea-level rise has con-tinued since then,the NGVD is now below the current day MSL along much of the U.S.Atlantic and Gulf coasts.At many locations,it is between the MSL and the MLLW.For accurate location of the NGVD relative to the MSL or MLLW,analysis with data from a local tide gage is required.For some harbor and coastal design,a staff gage is installed for recording water levels for a sustained period of time to confirm the relation between the local surveyor’s elevation datum,the assumed tidal datum,and the actual water surface elevation.Storm Surge n This can be defined broadly to include all the effects involved in a storm,inclu-ding wind stress across the continental shelf and within an estuary or body of water,barometric pressure,and wave-induced setup.The combined influence of these effects can change the water level by5to20ft depending on the intensity of the storm and coastal location.Engineers can use return-period analysis curves to estimate the likelihood of any particular elevation.The Federal Emergency Management Agency and the various Corps of Engineer Districts have developed such curves based on historic high-water-mark elevations and numerical models of the hydrodynamics of the continental shelf.23.4Coastal SedimentCharacteristicsMost beach sediments are sand.The day-to-day dynamics of the surf zone usually ensure that most fines,silts,and clays will be washed away to more quiescent locations offshore.Some beaches have layers of cobbles,rounded gravel,or shingles,flattened gravel.The size and composition of beach sands varies around the world and even along adjacent shore-lines.Essentially,the beach at any particular site consists of whatever loose material is available.Quartz is the most common mineral in beach sands. Other constituents in sands include feldspars and heavy minerals.Some beaches have significant por-tions of seashell fragments and some beaches are dominated by coral carbonate material.Beach sands are usually described in terms of grain-size distribution.The median diameter d50is a common measure of the central size of the distribution.The range of the distribution of sand sizes around this median is usually discussed in terms of sorting.The color of the sand depends primarily on the composition of the grains.The black sand beaches of Hawaii are derived from volcanic lava.The white sands of the panhandle of Florida are quartz that has developed a white color owing to mini-ature surface abrasions and bleaching.23.5Nearshore Currents andSand TransportAs wave energy enters the surf zone,some of the energy is transformed to nearshore currents and expended in sand movement.The nearshore cur-rentfield is dominated by the incident wave energy and the local windfield.The largest currents are the oscillatory currents associated with the waves. However,several forms of mean currents(long-shore currents,rip currents associated with nearshore circulation cells,and downwelling or upwelling associated with winds)can be important to sand transport.Longshore current is the mean current along the shore between the breaker line and the beach that is driven by an oblique angle of wave approach. The waves provide the power for the mean long-shore current and also provide the wave-by-wave agitation to suspend sand in the current.The resulting movement of sand is littoral drift or longshore sand transport.This process is referred to as a river of sand moving along the coast. Although the river-of-sand concept is an effective, simple explanation of much of the influence of engineering on adjacent beaches,the actual sand transport paths are more complex.This is par-ticularly so near inlets with large ebb-tidal shoals that influence the incident wave climate.Even on an open coast with straight and parallel offshore bottom contours,the longshore-sand-transport direction changes constantly in response to changes in the incident wave height,period,and Coastal and Port Engineering n23.9。

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a rXiv:h ep-th/035147v33Se p23A master equation for gravitational perturbations of maximally symmetric black holes in higher dimensions Hideo Kodama 1,∗)and Akihiro Ishibashi 2,∗∗)1Yukawa Institute for Theoretical Physics,Kyoto University Kyoto 606-8502,Japan 2D.A.M.T.P.,Centre for Mathematical Sciences,University of Cambridge Wilberforce Road,Cambridge CB30WA,United Kingdom We show that in four or more spacetime dimensions,the Einstein equations for gravita-tional perturbations of maximally symmetric vacuum black holes can be reduced to a single second-order wave equation in a two-dimensional static spacetime,irrespective of the mode of perturbations.Our starting point is the gauge-invariant formalism for perturbations in an arbitrary number of dimensions developed by the present authors,and the variable for the final second-order master equation is given by a simple combination of gauge-invariant variables in this formalism.Our formulation applies to the case of non-vanishing as well as vanishing cosmological constant Λ.The sign of the sectional curvature K of each spatial section of equipotential surfaces is also kept general.In the four-dimensional Schwarzschild background with Λ=0and K =1,the master equation for a scalar perturbation is identical to the Zerilli equation for the polar mode and the master equation for a vector perturba-tion is identical to the Regge-Wheeler equation for the axial mode.Furthermore,in the four-dimensional Schwarzschild-anti-de Sitter background with Λ<0and K =0,1,our equation coincides with those recently derived by Cardoso and Lemos.As a simple appli-cation,we prove the perturbative stability and uniqueness of four-dimensional non-extremal spherically symmetric black holes for any Λ.We also point out that there exists no simple relation between scalar-type and vector-type perturbations in higher dimensions,unlike in four dimension.Although in the present paper we treat only the case in which the hori-zon geometry is maximally symmetric,the final master equations are valid even when the horizon geometry is described by a generic Einstein manifold,if we employ an appropriate reinterpretation of the curvature K and the eigenvalues for harmonic tensors.§1.Introduction Perturbative analyses of four-dimensional black hole spacetimes have provideduseful tools for the investigation of astrophysical problems,such as gravitational wave emission from gravitational collapse and black holes,1),2),3)as well as for the investi-gation of more fundamental problems,such as the stability and uniqueness of black holes.1),4),5),6)In these analyses,a key role is played by the fact that the Einstein equations for perturbations can be reduced to a second-order ordinary differential equation (ODE)of the self-adjoint type through harmonic expansion.Such a master equation in the Schwarzschild background was first derived by Regge and Wheeler for the axial mode,7),8)and subsequently by Zerilli for the polar mode.9),10)Later,the formulation was further extended to the Kerr background by Teukolsky.11),12)Recently,it was also extended to the Schwarzschild-de Sitter and Schwarzschild-anti-de Sitter backgrounds by Cardoso and Lemos13),14)and utilised to determine the frequencies and the behaviour of quasi-normal modes.15),16),17),18),19) Judging from this experience in the four-dimensional case,it is expected that an extension of the formalism to higher dimensions would be quite useful for the inves-tigation of fundamental problems as well as phenomenological problems in higher-dimensional gravity theories,which are currently subjects of intensive research.In particular,such an extension will provide an exact basic equation for the quasi-normal mode analysis of higher-dimensional black holes20),21),17)motivated by the AdS/CFT issue.22)Such extensions already exist in some limited cases.For example,the present authors developed a gauge-invariant formalism for perturbations in spacetimes of arbitrary dimension greater than three in a previous paper23)(which is referred toas KIS2000in the present paper)by extending the formulation presented in Refs. 24)and25).There,assuming that the background spacetime of dimension n+m possesses a spatial isometry group G n that is isomorphic to the isometry groupof an n-dimensional space K n with constant sectional curvature K,we expanded perturbation variables in terms of harmonic tensors on K n and expressed the per-turbed Einstein equations as a set of equations for gauge-invariant variables in them-dimensional orbit space constructed from the expansion coefficients.In this for-malism,the gauge-invariant variables are grouped into three types,the tensor type, vector type,and scalar type,according to the type of harmonic tensors used to expand the perturbation variables.Each of these types of variables obeys an in-dependent closed set of equations.In particular,we showed that in the case thatm=2and the background spacetime satisfies the vacuum Einstein equations,the perturbed Einstein equations for both a vector perturbation and a tensor perturba-tion reduce to a single second-order wave equation—which is called a master equationin the present paper—in the two-dimensional orbit spacetime spanned by the time and radial coordinates.∗)This result is independent of the sign of K and holds for both vanishing and non-vanishing cosmological constantΛ.For a four-dimensional Schwarzschild black hole background,a vector perturba-tion corresponds to the axial(odd)mode,and the master variable and the master equation presented in KIS2000correspond directly to the Regge-Wheeler variable and the Regge-Wheeler equation,respectively.Hence,we already have an extensionto higher dimensions of the Regge-Wheeler formalism for the axial mode.However, such an extension for a scalar perturbation,i.e.,an extension to higher dimensions of the Zerilli formalism for the polar(even)mode in four dimensions,has not yet been obtained,although simple master equations have been derived for a scalar perturba-tion in constant curvature spacetimes using various methods.26),27),23),28),29),30),31),32),33) The main purpose of the present paper is to construct such an extension of the Zerilli formalism to spacetimes of arbitrary dimension greater than three.To be precise,we show that under the assumption of the G n symmetry of the backgroundspacetime,the gauge-invariant vacuum Einstein equations given in KIS2000for a scalar perturbation in a system of greater than three dimensions can be reduced to a single second-order wave equation in the two-dimensional orbit space for a master variableΦconsisting of a simple combination of the gauge-invariant variables.This equation is identical to the Zerilli equation for the polar mode in the four-dimensional Schwarzschild background.By the generalised Birkhofftheorem,the symmetry as-sumption requires the background spacetime to be static,and its metric is uniquely determined by the normalized curvature K of symmetry orbits,the cosmological constantΛ,and a parameter M representing the black hole mass,provided that the spacetime is not of the Nariai type,34)which is assumed in the present paper.In order to allow for the widest possible application of the present formulation,these parameters are kept arbitrary.For example,the formulation describes a scalar per-turbation of a higher-dimensional Schwarzschild black hole for K=1andΛ=0, while it describes a scalar perturbation of a Schwarzschild-anti-de Sitter spacetime forΛ<0and M=0.We also show that in the special case M=0,the master equation derived in the present paper is essentially equivalent to the master equation derived by Mukohyama in Ref.29).Further,for completeness,we show explicitly that vector and tensor perturbations obey master equations whose structures are the same as in the case of a scalar perturbation,and we give the corresponding effective potentials for these equations.We also point out that the simple relation between the polar mode and the axial mode,which wasfirst obtained by Chan-drasekhar and Detweiler1)for a four-dimensional Schwarzschild black hole and then extended to the four-dimensional asymptotically anti-de Sitter case by Cardoso and Lemos,13),14)does not hold in higher dimensions.The present paper is organized as follows.In the next section,we show that the gauge-invariant perturbation equations for a scalar perturbation given in KIS2000 are equivalent to a set offirst-order ODEs with a linear constraint for three gauge-invariant variables,after carrying out the Fourier transform with respect to the time coordinate.Then,in§3,this set of equations is reduced to a single master equation of the Zerilli type in the case of a non-vanishing frequency.We further show that this master equation can be converted into a wave equation for a masterfieldΦin the two-dimensional orbit space by the inverse Fourier transformation and that all gauge-invariant variables can be represented as combinations of thisfield and its derivatives.A subtle point regarding static perturbations in this derivation is treated in§4.In §5,we rewrite the master equations for tensor and vector perturbations given in KIS2000in the same form as that for a scalar perturbation.Section6is devoted to discussion.There,using the master equations for four dimensions,the perturbative stability and uniqueness of the Schwarzschild-de Sitter and Schwarzschild-anti de-Sitter black holes in four dimensions is proved.We also discuss the relation between the scalar and vector master variables and the extension of the formulation to the case in which the horizon geometry is described by a generic Einstein metric.Because the calculations required to derive the master equations are quite lengthy,most of them were done by symbolic computation with Maple.§2.Basic equationsIn this section,we show that the gauge-invariant equations for scalar pertur-bations given in KIS2000reduce to a set offirst-order differential equations with a linear constraint for three gauge-invariant variables in a maximally symmetric black hole background.2.1.Perturbation equationsThe general form of the metric of a G n-symmetric background spacetime con-sidered in the present paper is given byds2=g ab(y)dy a dy b+r2(y)dσ2n,(2.1)where g ab is the Lorentzian metric of the two-dimensional orbit spacetime,and dσ2n=γij(z)dz i dz j is the metric of the n-dimensional G n-invariant base space K n with normalized constant sectional curvature K=0,±1.Hence,the dimension of the whole spacetime is n+2,and the spherically symmetric case corresponds to K=1.Scalar perturbations of this spacetime can be expanded in terms of the harmonic functions S on K n,which satisfy the equation(ˆ△n+k2)S=0,(2.2) whereˆ△n is the Laplace-Beltrami operator on K n,and k2is its eigenvalue.For K=1,k2takes discrete values,k2=l(l+n−1),l=0,1,2,···,(2.3)while for K≤0,k2can take any non-negative real value.Each harmonic mode of the metric perturbationδg MN can be writtenδg ab=f ab S,δg ai=rf a S i,δg ij=2r2(H Lγij S+H T S ij),(2.4)whereS i=−1k2ˆDiˆDj S+1Birkhofftheorem,we do not have to consider this case.Next,k2=nK occurs only for K=1,and this corresponds to l=1.For such modes,S ij vanishes,and the vari-able H T is not defined.We show below that these modes have no physical degrees of freedom.For modes with k2(k2−nK)=0,the following combinations provide a basis for gauge-invariant variables for metric perturbations of the scalar type:23)F=H L+1rD a rX a,(2.7a)F ab=f ab+D a X b+D b X a.(2.7b) Here,D a represents the covariant derivative with respect to the metric g ab in the two-dimensional orbit space,and X a is given byX a=rkD a H T .(2.8)Because the Einstein tensors G MN have the same structure as the metric per-turbation(2.4)under the harmonic expansion,the vacuum Einstein equations for a scalar perturbation are given by the following set of equations:˜Eab≡r n−2E ab=0,˜E a≡r n−2E a=0,˜E L≡r n−2E L=0,˜E T≡r n−2E T=0.(2.9) The explicit expressions of E ab,E a,E L and E T in terms of the gauge-invariant vari-ables(2.7)can be obtained by specializing the general formula given by(63)–(66)in KIS2000to the case in which the orbit space is two-dimensional(m=2).As these expressions are long,we give them in Appendix A.The equations in(2.9)are not independent,due to the Bianchi identities,which are written1r ˜EL+n−1kr˜ET=0,(2.10a)1r ˜Ea−nD a r2.2.Fourier transformationBecause solutions to the vacuum Einstein equations with the spatial symmetry G n are always static as asserted by the Birkhofftheorem,our background metric can take the formds2=−f(r)dt2+dr2r n−1−λr2,(2.15) provided that the spacetime is not of the Nariai type,which is assumed in the present paper.Here,λis related to the cosmological constantΛbyλ=2Λ8πG,(2.17)where A n=2π(n+1)/2/Γ[(n+1)/2]is the area of a unit n-sphere and G denotes the n+2-dimensional Newton constant.Because the non-vanishing connection coefficients for this metric are given byΓt tr=f′2,Γr rr=−f′2f˜E rr−r2f′∗)It is known that,in higher dimensions,the metric(2.14)with(2.15)can describe many different black hole solutions to the vacuum Einstein equations,with the simple replacement of dσ2n by the metric for any Einstein manifold.35),36)Among such solutions,the G n-symmetric metric is the maximally symmetric solution.Our formulation also holds in the case that dσ2n is given by a generic Einstein metric,as mentioned in§6.Next,we reduce these equations to first-order ODEs for three variables.First,let us introduce the variables X,Y and Z byX =˜F t t −2˜F ,Y =˜F r r −2˜F ,Z =˜F r t .(2.20)Then,from (2.11),all basic gauge-invariant variables can be expressed in terms of these three variables asF t t =(n −1)X −Ynr n −2,F r t =Z 2nr n −2.(2.21b)Inserting these expressions into (2.12),we obtain(2r/k )˜Et ≡−∂t X −∂r Z =0,(2.22a)(2r/k )˜E r ≡f ′2f Y +1rX + f ′rY + k 2f 2 ˜Z,(2.24a)Y ′=f ′f 2˜Z,(2.24b)˜Z ′=X,(2.24c)ω2r 2+Kλr 2+M r n −1 X+ ω2r 2−k 2f +nK 2−(n −1)Kλr 2−4nKM r 2(n −1)Y−1r n −1 k 2 ˜Z =0.(2.24d)Here,the last equation corresponds to −2r 2f ˜Er r =0.Now,we comment on the l =1mode.As explained in Appendix B,the above basic equations also hold for this mode,if we regard E T =0as a gauge condition.However,the number of the residual gauge degrees of freedom that remain after this partial gauge fixing is the same as that of the degrees of freedom of the general solution to (2.24).This implies that there exist no physical degrees of freedom for l =1.For this reason,we assume that l ≥2from this point.§3.Master equationBecause the constraint(2.24d)is linear,we can always reduce the system offirst-order ODEs(2.24)to a second-order ODE for any linear combination of X,Y and Z. However,the corresponding2nd-order ODE in general has coefficients that depend on the frequencyωin an intricate way and therefore it is not useful.In particular, in order to allow for its use in the stability analysis of black holes,it is desirable that the master equation has the form AΦ=ω2Φ,where A is a self-adjoint second-order ordinary differential operator independent ofω,as does the Zerilli equation for the four-dimensional Schwarzschild black hole.Starting from the expression of the master variable for the Zerilli equation in terms of our gauge-invariant variables, after some trial and error,we have found that the following form ofΦis the best:n˜Z−r(X+Y)Φ:=n(n+1)x;(3.2)2m=k2−nK,(3.3)2Mx=dr f dΦ,(3.6)16r2H2withQ(r)=− n3(n+2)(n+1)2x2−12n2(n+1)(n−2)mx+4(n−2)(n−4)m2 y +n4(n+1)2x3+n(n+1) 4(2n2−3n+4)m+n(n−2)(n−4)(n+1)K x2−12n[(n−4)m+n(n+1)(n−2)K]mx+16m3+4Kn(n+2)m2,(3.7) wherey=λr2.(3.8) It is easy to see that this equation is identical to the Zerilli equation9)for n=2, K=1andλ=0and identical to the equation for even modes derived by Cardoso and Lemos13),14)for n=2,K=0,1andλ<0.The original fundamental variables X,Y and Z are expressed in terms of the master variableΦasX=r n/2−2 ω2r216H2 Φ+Q XY =r n/2−2 −ω2r 216H 2 Φ+Q Y 4H Φ−fr∂r Φ .(3.9c)Here,the coefficients P X ,Q X ,P Y ,Q Y ,and P Z are functions of r expressed in terms of x =2M/r n −1and y =λr 2asP X (r )=4(n −1)[n 2(n +1)x −2(n −2)m ]my+n 3(n +1)3x 3+2n (n +1)[2(n 2+n +2)m −n (n −2)(n +1)K ]x 2−4n [(n −11)m +n (n +1)(n −3)K ]mx +16m 3+8Km 2n 2,(3.10a)Q X (r )=4(n −1)my +n (n +1)2x 2+2[(3n −1)m −n (n +1)K ]x−4Knm,(3.10b)P Y (r )=[2n 4(n +1)2x 2−4n 2(n +1)(n −3)mx +(−8n +16)m 2]y+n 3(n −1)(n +1)2x 3+2n (n 2−1)[4m −n (n −2)(n +1)K ]x 2+4n (n −1)[3m +n (n +1)K ]mx,(3.10c)Q Y (r )=2[n 2(n +1)x +2m ]y +n (n −1)(n +1)x 2−2(n −1)[m +n (n +1)K ]x,(3.10d)P Z (r )=[−n 2(n +1)x +2(n −2)m ]y +n (n +1)x 2+[2(2n −1)m +n (n +1)(n −2)K ]x −2Knm.(3.10e)Although we have utilized the Fourier transformation with respect to the time coordinate to derive the master equation (3.5),we can apply the inverse Fourier transform to it and thereby obtain the master equation in the form of a wave equation for a master field Φ(t,r )in the two-dimensional orbit space with the coordinates (t,r ).This master wave equation is obtained simply replacing ωby i∂t in (3.5).This yields2Φ−V S f ∂2t Φ−P X 4Hr∂r Φ ,(3.12a)Y =r n/2−2 r 216H2Φ+Q Y 4H ∂t Φ+fr∂r ∂t Φ .(3.12c)If we introduce the variable ˜Ωdefined by ˜Ω=r n/2HΦ,(3.13)these expressions can be put into the covariant form ∗)˜F =1HD a D b ˜Ω−1r n/2−1H,(3.15)we can obtain the time derivative of the master wave equation,∂t 2Φ−V S ∗)We would like to thank an anonymous referee for recommending us to look for these covariantexpressions.given in the previous section does not apply to static perturbations.In this section,we show that in spite of this,the master wave equation (3.11)alsodescribes staticscalar perturbations.For static perturbations,from (2.22a),(2.22a),(A .2a)and (A .2b),we find thatthe equations E a =0,E r t =0and E r r=0can be written E t :Z ′=0,(4.1a)E r :Y ′+f ′r 2Z =0,(4.1c)E r r:−f ′r 2(f −K )+2(n +1)λ2r+f ′′2+nfr 2K +fn+(3n −2)f ′nf ′′−k 2r 2(f −K )+4(n +1)λr−(f ′)2nX−2(f −K )nλ+2(n −1)2f+2(n −1)r 2Y,(4.2a)Y ′=f ′2k 2r n/2−1f ′(r )H (r ).(4.3)For this choice,if we express X and Y in terms of Φand ∂r Φwith the help of (4.2),we find that they are represented by (3.12a)and (3.12b)with ∂t Φ=0.Further,insertion of these expressions into (4.2)gives (3.11)without the time derivative term.Thus,it is found that the same master equation holds for both non-static and static perturbations.Although it is preferable for the investigation of general cases(such as the stabil-ity analysis of black holes)that every perturbation be described by a single master equation,the potential in the master equation(3.11)is rather complicated and is not always useful for analysis of static perturbations.Because the behaviour of static perturbations is important with regard to the issue of black hole uniqueness,it would be useful if we could obtain a master equation with a simpler potential.Now,we show that such a master equation is indeed obtained if we adopt Y as the master variable.First,(4.2)leads to the following second-order ODE for Y:Y′′+αY′+βY=0,(4.4) wherer2ff′α=(n−1)(n+2)Kx+2nKλr2+(n−1)(n−4)x2−(n2+11n−10)xλr2−2(n−4)λ2r4,(4.5a) r2fβ=−k2+nK+(n−2)(K−f).(4.5b) In order to rewrite this equation in a formally self-adjoint form,we introduce the new variable˜Y defined by˜Y:=SY;(4.6)S=f−1/2exp αr n/2−1f′.(4.7) Then,the above equation for Y is transformed into−f d dr +˜V˜Y=0,(4.8) where˜V(r)=f;(4.9)4r2(rf′)2˜Q(r)=−(2n−1)(n−1)2x4+2(n−1)[n(n−1)K+(5n2+23n+6)y]x3+[n(n−2)(n−1)2K2−2(n−1)(n+3)(n2+10n+6)Ky+(n4+28n3+61n2−66n−28)y2]x2+[4(n−1)(3n2+10n+4)K2−8(3n3+7n2−5n−6)Ky+4(3n3+7n2−12n−4)y2]yx+4n(n−2)K2y2−8(n2−2n−2)Ky3+4n(n−2)y4.(4.10) The dependence on k2of this effective potential is simpler than that of V.Further-more,although it is still rather complicated forλ=0,it becomes quite simple for λ=0:˜V=4k2(1−x)+n(n−2)+2nx−(2n−1)x2§5.Vector and tensor perturbationsIt was shown in KIS2000that vector and tensor perturbations in the background spacetimes considered in the present paper are described by master equations of the wave equation type in the two-dimensional orbit space.In this section,forcompleteness,we show that these equations can also be written in the form of (3.11).5.1.Tensor perturbationsPerturbations of the tensor type can be expanded in terms of the tensor-type harmonic tensors T ij satisfying(ˆ△n +k 2T)T ij =0,(5.1a)T i i =0,ˆDj T j i =0.(5.1b)The eigenvalues k 2Tare all positive.They form a continuous set for K ≤0and a discrete set,k 2T =l (l +n −1)−2,l =1,2,···,(5.2)for K =1.Each harmonic component of the metric perturbation is expressed by (2.4),with f ab =f a =H L =0and S ij replaced by T ij .H T is gauge-invariant by itself,and in vacuum,it satisfies the following wave equation in the two-dimensional orbit space:2H T +nr 2H T =0.(5.3)If we introduce the master variable ΦbyΦ=r n/2H T ,(5.4)this equation can be rewritten in the same form as (3.11):2Φ−V Tr 2k 2T+2K +n (n −2)4λr 2+n 2M∗)The authors thank Sean Hartnoll for discussion of this point 39)5.2.Vector perturbationsPerturbations of the vector type can be expanded in terms of the vector-type harmonic tensors V i satisfying(ˆ△n+k2V)V i=0,(5.7a)ˆDj Vj=0.(5.7b) As in the case of the tensor-type harmonics,the eigenvalues k2V are all positive, forming a continuous set for K≤0and a discrete set for K=1.However,this discrete spectrum is shifted by unity with respect to that in the tensor case:k2V=l(l+n−1)−1,l=1,2,···.(5.8) The expression for the metric perturbation is now given by(2.4)with S i replaced by V i and S ij byV ij=−1k VD a H T(5.10)is gauge invariant and represents a natural basic variable.In our vacuum background, F a is expressed in terms of afieldΩ(t,r)in the two-dimensional orbit space satisfying the wave equation2Ω−nr2Ω=0(5.11)asr n−1F a=ǫab D bΩ,(5.12) whereǫab is the Levi-Civita tensor of the two-dimensional orbit space.If we introduce the master variableΦbyΦ=r−n/2Ω,(5.13) (5.11)takes the form2Φ−V Vr2 k2V+K+n(n−2)K4λr2−3n2MFor k2V=(n−1)K,i.e.,K=1and l=1,V ij vanishes,and the perturbation vari-able H T loses meaning.In this case,the following becomes a basic gauge-invariant variable:F(1)ab=rD a(f b/r)−rD b(f a/r).(5.16)In our vacuum background,from the Einstein equations,it follows that F(1)ab is ex-pressed asF(1) ab =Lǫabself-adjoint extension in the L2-space with respect to the inner product(Φ1,Φ2)L2= dr∗Φ∗1(r)Φ2(r).(6.2) In this case,we must impose a boundary condition at r=∞to make the problem well-posed.The most natural choice is to require thatΦvanish at r=∞,if we are concerned with the local stability of the black hole.Under this boundary condition, we can apply the same reasoning as for the Schwarzschild-de Sitter black hole,and we therebyfind that the Schwarzschild-anti-de Sitter black hole is stable.We can also undertake a similar analysis for vector perturbations of these four-dimensional black holes,although the situation in this case is slightly subtle.Here, the effective potential becomesV V=fr+6+l2(l2+5) .(6.3)ForΛ≥0,this is positive definite for l≥2outside the horizon from1−2M/r= f+λr2>0.Hence,the argument given above again applies.In contrast,forΛ<0, V V becomes negative near the horizon for large|λ|,and the above argument does not apply.Nevertheless,we can prove using the somewhat sophisticated argument given in Ref.41)that there exists no unstable mode in this case as well.From the above considerations,we have established the perturbative stability of spherically symmetric black holes in four dimensions,irrespective of the sign of the cosmological constant.The above argument also proves the uniqueness of these black holes in a perturbative sense,because there should exist a regular static solution to the perturbation equation with l≥1if there exists a continuous family of regular static black hole solutions with the same mass that contains the spherically symmetric solutions.In spacetimes of dimension greater than four,the stability of spherically sym-metric black holes has not yet been investigated,even in the asymptoticallyflat case. It seems that our formulation would be useful in the investigation of this problem. For example,using our formulation,we can prove the stability of higher-dimensional Schwarzschild black holes,as will be shown in a separate paper.41)This is not as trivial as in the four-dimensional case discussed above,because the effective poten-tials in the master equations are not positive definite in general for vector and scalar perturbations.Nevertheless,it can be shown that the differential operators on the left-hand sides of(3.5)and(5.14)have unique positive self-adjoint extensions.A similar technique might be used to analyse the asymptotically de Sitter and anti-de Sitter cases in higher dimensions as well,although the behaviour of the potential in these cases is much more complicated.This problem is now under investigation.Next,we comment on the relation between the master variable for a scalar perturbation and that for a vector perturbation,which we here denoteΦS andΦV, respectively.In the four-dimensional Schwarzschild background withΛ=0and K=1,Chandrasekhar and Detweiler found that they are related by the simple relationΦS=pΦV+qΦ′V,(6.4)where p and q are appropriate functions of r that are independent of the frequency ωif and only if the corresponding effective potentials are expressed in terms of a single function F of r independent ofωasdFV S,V V=±fby a generic Einstein manifold.AI is a JSPS fellow,and HK is supported by the JSPS grant No.15540267.Appendix AWe have the following:2E ab =− F ab +D a D c F cb +D b D c F ca+nD c rr 2+2R (2)−4rD a rD b F +1rD c rD d F cd +2nr 2D c rD d rF cd −2n F −2n (n +1)r 2F− F c c −nr 2+1k E a =−1rF b b+2(n −1)D a F,(A .1b)2E L =−D a D b Fab−2(n −1)r 2 (n −2)D a rD b r +2rD a D brF ab+ F c c +n −1nk 22R(2)F c c +2(n −1) F +2n (n −1)nr 2F,(A .1c)2r 2r 2−f ′′−nf ′r−f ′r +f ′f∂2t X−f ′+ n −1nλ+(n +2)f ′n X+12+nfr 2−2(n 2−1)2rf ′−n −1r 2Y+2nrf −f ′r 2K −(2n −3)f nλ+n −2n f ′′−k 22+4fr 2K −n −3nλ+(n −2)f ′nY.(A .2c)Here,λ=2Λ2f∂2t X+f ′2nr 2+(6n −4−n 2)f ′2n X−f4+f2nr 2+(−n 2+2n −4)f ′2nY+12f2∂t Z +1The l =1mode in the spherically symmetric caseas¯δFab=−2rk Dr·DL+(n−2)k2k ¯δET=1nr2L.(B.3)From this,it follows that we can always make E T vanish by choosing an appropriate gauge.This requirement does notfix the gauge completely,and there remain resid-ual gauge degrees of freedom parametrized by two arbitrary functions of the space coordinate r in the two-dimensional orbit spacetime(t,r).Appendix CThe master variableΦ(S)in Ref.29)andΩ(=Φ(S))in KIS2000for scalarperturbations are related to the gauge-invariant variables by˜F=1n 2+1−2rDr·DΩ− k2−nK√√f.(C.5) Because it is easily checked thatΩ=r n/2Φsatisfies(C.2),this relation implies that C(t)√r2 C.(C.6)。

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