Part II-1 Water Wave Mechanics
Total Page:16
File Type:pdf, Size:1020Kb
Load more
Recommended publications
-
Well-Balanced Schemes for the Shallow Water Equations with Coriolis Forces
Well-balanced schemes for the shallow water equations with Coriolis forces Alina Chertock, Michael Dudzinski, Alexander Kurganov & Mária Lukáčová- Medvid’ová Numerische Mathematik ISSN 0029-599X Volume 138 Number 4 Numer. Math. (2018) 138:939-973 DOI 10.1007/s00211-017-0928-0 1 23 Your article is protected by copyright and all rights are held exclusively by Springer- Verlag GmbH Germany, part of Springer Nature. This e-offprint is for personal use only and shall not be self-archived in electronic repositories. If you wish to self-archive your article, please use the accepted manuscript version for posting on your own website. You may further deposit the accepted manuscript version in any repository, provided it is only made publicly available 12 months after official publication or later and provided acknowledgement is given to the original source of publication and a link is inserted to the published article on Springer's website. The link must be accompanied by the following text: "The final publication is available at link.springer.com”. 1 23 Author's personal copy Numer. Math. (2018) 138:939–973 Numerische https://doi.org/10.1007/s00211-017-0928-0 Mathematik Well-balanced schemes for the shallow water equations with Coriolis forces Alina Chertock1 · Michael Dudzinski2 · Alexander Kurganov3,4 · Mária Lukáˇcová-Medvid’ová5 Received: 28 April 2014 / Revised: 19 September 2017 / Published online: 2 December 2017 © Springer-Verlag GmbH Germany, part of Springer Nature 2017 Abstract In the present paper we study shallow water equations with bottom topog- raphy and Coriolis forces. The latter yield non-local potential operators that need to be taken into account in order to derive a well-balanced numerical scheme. -
Accurate Modelling of Uni-Directional Surface Waves
Journal of Computational and Applied Mathematics 234 (2010) 1747–1756 Contents lists available at ScienceDirect Journal of Computational and Applied Mathematics journal homepage: www.elsevier.com/locate/cam Accurate modelling of uni-directional surface waves E. van Groesen a,b,∗, Andonowati a,b,c, L. She Liam a, I. Lakhturov a a Applied Mathematics, University of Twente, The Netherlands b LabMath-Indonesia, Bandung, Indonesia c Mathematics, Institut Teknologi Bandung, Indonesia article info a b s t r a c t Article history: This paper shows the use of consistent variational modelling to obtain and verify an Received 30 November 2007 accurate model for uni-directional surface water waves. Starting from Luke's variational Received in revised form 3 July 2008 principle for inviscid irrotational water flow, Zakharov's Hamiltonian formulation is derived to obtain a description in surface variables only. Keeping the exact dispersion Keywords: properties of infinitesimal waves, the kinetic energy is approximated. Invoking a uni- AB-equation directionalization constraint leads to the recently proposed AB-equation, a KdV-type Surface waves of equation that is also valid on infinitely deep water, that is exact in dispersion for Variational modelling KdV-type of equation infinitesimal waves, and that is second order accurate in the wave height. The accuracy of the model is illustrated for two different cases. One concerns the formulation of steady periodic waves as relative equilibria; the resulting wave profiles and the speed are good approximations of Stokes waves, even for the Highest Stokes Wave on deep water. A second case shows simulations of severely distorting downstream running bi-chromatic wave groups; comparison with laboratory measurements show good agreement of propagation speeds and of wave and envelope distortions. -
Transport Due to Transient Progressive Waves of Small As Well As of Large Amplitude
This draft was prepared using the LaTeX style file belonging to the Journal of Fluid Mechanics 1 Transport due to Transient Progressive Waves Juan M. Restrepo1,2 , Jorge M. Ram´ırez 3 † 1Department of Mathematics, Oregon State University, Corvallis OR 97330 USA 2Kavli Institute of Theoretical Physics, University of California at Santa Barbara, Santa Barbara CA 93106 USA. 3Departamento de Matem´aticas, Universidad Nacional de Colombia Sede Medell´ın, Medell´ın Colombia (Received xx; revised xx; accepted xx) We describe and analyze the mean transport due to numerically-generated transient progressive waves, including breaking waves. The waves are packets and are generated with a boundary-forced air-water two-phase Navier Stokes solver. The analysis is done in the Lagrangian frame. The primary aim of this study is to explain how, and in what sense, the transport generated by transient waves is larger than the transport generated by steady waves. Focusing on a Lagrangian framework kinematic description of the parcel paths it is clear that the mean transport is well approximated by an irrotational approximation of the velocity. For large amplitude waves the parcel paths in the neighborhood of the free surface exhibit increased dispersion and lingering transport due to the generation of vorticity. Armed with this understanding it is possible to formulate a simple Lagrangian model which captures the transport qualitatively for a large range of wave amplitudes. The effect of wave breaking on the mean transport is accounted for by parametrizing dispersion via a simple stochastic model of the parcel path. The stochastic model is too simple to capture dispersion, however, it offers a good starting point for a more comprehensive model for mean transport and dispersion. -
Arxiv:2002.03434V3 [Physics.Flu-Dyn] 25 Jul 2020
APS/123-QED Modified Stokes drift due to surface waves and corrugated sea-floor interactions with and without a mean current Akanksha Gupta Department of Mechanical Engineering, Indian Institute of Technology, Kanpur, U.P. 208016, India.∗ Anirban Guhay School of Science and Engineering, University of Dundee, Dundee DD1 4HN, UK. (Dated: July 28, 2020) arXiv:2002.03434v3 [physics.flu-dyn] 25 Jul 2020 1 Abstract In this paper, we show that Stokes drift may be significantly affected when an incident inter- mediate or shallow water surface wave travels over a corrugated sea-floor. The underlying mech- anism is Bragg resonance { reflected waves generated via nonlinear resonant interactions between an incident wave and a rippled bottom. We theoretically explain the fundamental effect of two counter-propagating Stokes waves on Stokes drift and then perform numerical simulations of Bragg resonance using High-order Spectral method. A monochromatic incident wave on interaction with a patch of bottom ripple yields a complex interference between the incident and reflected waves. When the velocity induced by the reflected waves exceeds that of the incident, particle trajectories reverse, leading to a backward drift. Lagrangian and Lagrangian-mean trajectories reveal that surface particles near the up-wave side of the patch are either trapped or reflected, implying that the rippled patch acts as a non-surface-invasive particle trap or reflector. On increasing the length and amplitude of the rippled patch; reflection, and thus the effectiveness of the patch, increases. The inclusion of realistic constant current shows noticeable differences between Lagrangian-mean trajectories with and without the rippled patch. -
NANOOS Asset List 1 National Oceanic and Atmospheric
NANOOS Asset List 2008 NANOOS Asset List 1 National Oceanic and Atmospheric Administration 1.1 The CoastWatch West Coast Regional Node http://coastwatch.pfel.noaa.gov Daily – Monthly composites of satellite observations Sea Surface Temperature (GOES & POES) Ocean Color (MODIS and SeaWiFS) Ocean Winds (QuikSCAT) 1.2 The National Data Buoy Center http://seaboard.ndbc.noaa.gov/maps/Northwest.shtml 6 Minute – Hourly buoy observations Meteorological Observations (Air Temp., Pressure, Wind Speed and Direction) Ocean Observations (Water Temp., Wave Height, Period and Direction) 1.3 The Center for Operational Oceanographic Products and Services http://tidesandcurrents.noaa.gov http://opendap.co-ops.nos.noaa.gov/content 6 Minute near-shore station observations Meteorological Observations (Air Temp., Pressure, Wind Speed and Direction) Ocean Observations (Water Temp., Water Level) 1.4 NOAAWatch http://www.noaawatch.gov Information related to ongoing environmental events NOAAWatch themes include Air Quality, Droughts, Earthquakes, Excessive Heat, Fire, Flooding, Harmful Algal Blooms (HABs), Oil Spills, Rip Currents, Severe Weather, Space Weather, Tsunamis, and Volcanoes 1.5 National Weather Service http://www.weather.gov Environmental observations and forecasts Coastal and Marine Forecasts Weather Warnings 1 NANOOS Asset List 2008 Surface Pressure Maps Coastal and Marine Observations (Wind, Visibility, Sky Conditions, Temperature, Dew Point, Relative Humidity, Atmospheric Pressure, Pressure tendency) GOES Satellite Observations (Visible, -
The Stokes Drift in Ocean Surface Drift Prediction
EGU2020-9752 https://doi.org/10.5194/egusphere-egu2020-9752 EGU General Assembly 2020 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. The Stokes drift in ocean surface drift prediction Michel Tamkpanka Tamtare, Dany Dumont, and Cédric Chavanne Université du Québec à Rimouski, Institut des Sciences de la mer de Rimouski, Océanographie Physique, Canada ([email protected]) Ocean surface drift forecasts are essential for numerous applications. It is a central asset in search and rescue and oil spill response operations, but it is also used for predicting the transport of pelagic eggs, larvae and detritus or other organisms and solutes, for evaluating ecological isolation of marine species, for tracking plastic debris, and for environmental planning and management. The accuracy of surface drift forecasts depends to a large extent on the quality of ocean current, wind and waves forecasts, but also on the drift model used. The standard Eulerian leeway drift model used in most operational systems considers near-surface currents provided by the top grid cell of the ocean circulation model and a correction term proportional to the near-surface wind. Such formulation assumes that the 'wind correction term' accounts for many processes including windage, unresolved ocean current vertical shear, and wave-induced drift. However, the latter two processes are not necessarily linearly related to the local wind velocity. We propose three other drift models that attempt to account for the unresolved near-surface current shear by extrapolating the near-surface currents to the surface assuming Ekman dynamics. Among them two models consider explicitly the Stokes drift, one without and the other with a wind correction term. -
Downloaded 09/24/21 11:26 AM UTC 966 JOURNAL of PHYSICAL OCEANOGRAPHY VOLUME 46
MARCH 2016 G R I M S H A W E T A L . 965 Modelling of Polarity Change in a Nonlinear Internal Wave Train in Laoshan Bay ROGER GRIMSHAW Department of Mathematical Sciences, Loughborough University, Loughborough, United Kingdom CAIXIA WANG AND LAN LI Physical Oceanography Laboratory, Ocean University of China, Qingdao, China (Manuscript received 23 July 2015, in final form 29 December 2015) ABSTRACT There are now several observations of internal solitary waves passing through a critical point where the coefficient of the quadratic nonlinear term in the variable coefficient Korteweg–de Vries equation changes sign, typically from negative to positive as the wave propagates shoreward. This causes a solitary wave of depression to transform into a train of solitary waves of elevation riding on a negative pedestal. However, recently a polarity change of a different kind was observed in Laoshan Bay, China, where a periodic wave train of elevation waves converted to a periodic wave train of depression waves as the thermocline rose on a rising tide. This paper describes the application of a newly developed theory for this phenomenon. The theory is based on the variable coefficient Korteweg–de Vries equation for the case when the coefficient of the quadratic nonlinear term undergoes a change of sign and predicts that a periodic wave train will pass through this critical point as a linear wave, where a phase change occurs that induces a change in the polarity of the wave, as observed. A two-layer model of the density stratification and background current shear is developed to make the theoretical predictions specific and quantitative. -
Title Relation Between Wave Characteristics of Cnoidal Wave
Relation between Wave Characteristics of Cnoidal Wave Title Theory Derived by Laitone and by Chappelear Author(s) YAMAGUCHI, Masataka; TSUCHIYA, Yoshito Bulletin of the Disaster Prevention Research Institute (1974), Citation 24(3): 217-231 Issue Date 1974-09 URL http://hdl.handle.net/2433/124843 Right Type Departmental Bulletin Paper Textversion publisher Kyoto University Bull. Disas. Prey. Res. Inst., Kyoto Univ., Vol. 24, Part 3, No. 225,September, 1974 217 Relation between Wave Characteristics of Cnoidal Wave Theory Derived by Laitone and by Chappelear By Masataka YAMAGUCHIand Yoshito TSUCHIYA (Manuscriptreceived October5, 1974) Abstract This paper presents the relation between wave characteristicsof the secondorder approxi- mate solutionof the cnoidal wave theory derived by Laitone and by Chappelear. If the expansionparameters Lo and L3in the Chappeleartheory are expanded in a series of the ratio of wave height to water depth and the expressionsfor wave characteristics of the secondorder approximatesolution of the cnoidalwave theory by Chappelearare rewritten in a series form to the second order of the ratio, the expressions for wave characteristics of the cnoidalwave theory derived by Chappelearagree exactly with the ones by Laitone, whichare convertedfrom the depth below the wave trough to the mean water depth. The limitingarea betweenthese theories for practical applicationis proposed,based on numerical comparison. In addition, somewave characteristicssuch as wave energy, energy flux in the cnoidal waves and so on are calculated. 1. Introduction In recent years, the various higher order solutions of finite amplitude waves based on the perturbation method have been extended with the progress of wave theories. For example, systematic deviations of the cnoidal wave theory, which is a nonlinear shallow water wave theory, have been made by Kellern, Laitone2), and Chappelears> respectively. -
Waves and Weather
Waves and Weather 1. Where do waves come from? 2. What storms produce good surfing waves? 3. Where do these storms frequently form? 4. Where are the good areas for receiving swells? Where do waves come from? ==> Wind! Any two fluids (with different density) moving at different speeds can produce waves. In our case, air is one fluid and the water is the other. • Start with perfectly glassy conditions (no waves) and no wind. • As wind starts, will first get very small capillary waves (ripples). • Once ripples form, now wind can push against the surface and waves can grow faster. Within Wave Source Region: - all wavelengths and heights mixed together - looks like washing machine ("Victory at Sea") But this is what we want our surfing waves to look like: How do we get from this To this ???? DISPERSION !! In deep water, wave speed (celerity) c= gT/2π Long period waves travel faster. Short period waves travel slower Waves begin to separate as they move away from generation area ===> This is Dispersion How Big Will the Waves Get? Height and Period of waves depends primarily on: - Wind speed - Duration (how long the wind blows over the waves) - Fetch (distance that wind blows over the waves) "SMB" Tables How Big Will the Waves Get? Assume Duration = 24 hours Fetch Length = 500 miles Significant Significant Wind Speed Wave Height Wave Period 10 mph 2 ft 3.5 sec 20 mph 6 ft 5.5 sec 30 mph 12 ft 7.5 sec 40 mph 19 ft 10.0 sec 50 mph 27 ft 11.5 sec 60 mph 35 ft 13.0 sec Wave height will decay as waves move away from source region!!! Map of Mean Wind -
Sea State in Marine Safety Information Present State, Future Prospects
Sea State in Marine Safety Information Present State, future prospects Henri SAVINA – Jean-Michel LEFEVRE Météo-France Rogue Waves 2004, Brest 20-22 October 2004 JCOMM Joint WMO/IOC Commission for Oceanography and Marine Meteorology The future of Operational Oceanography Intergovernmental body of technical experts in the field of oceanography and marine meteorology, with a mandate to prepare both regulatory (what Member States shall do) and guidance (what Member States should do) material. TheThe visionvision ofof JCOMMJCOMM Integrated ocean observing system Integrated data management State-of-the-art technologies and capabilities New products and services User responsiveness and interaction Involvement of all maritime countries JCOMM structure Terms of Reference Expert Team on Maritime Safety Services • Monitor / review operations of marine broadcast systems, including GMDSS and others for vessels not covered by the SOLAS convention •Monitor / review technical and service quality standards for meteo and oceano MSI, particularly for the GMDSS, and provide assistance and support to Member States • Ensure feedback from users is obtained through appropriate channels and applied to improve the relevance, effectiveness and quality of services • Ensure effective coordination and cooperation with organizations, bodies and Member States on maritime safety issues • Propose actions as appropriate to meet requirements for international coordination of meteorological and related communication services • Provide advice to the SCG and other Groups of JCOMM on issues related to MSS Chair selected by Commission. OPEN membership, including representatives of the Issuing Services for GMDSS, of IMO, IHO, ICS, IMSO, and other user groups GMDSS Global Maritime Distress & Safety System Defined by IMO for the provision of MSI and the coordination of SAR alerts on a global basis. -
SWAN Technical Manual
SWAN TECHNICAL DOCUMENTATION SWAN Cycle III version 40.51 SWAN TECHNICAL DOCUMENTATION by : The SWAN team mail address : Delft University of Technology Faculty of Civil Engineering and Geosciences Environmental Fluid Mechanics Section P.O. Box 5048 2600 GA Delft The Netherlands e-mail : [email protected] home page : http://www.fluidmechanics.tudelft.nl/swan/index.htmhttp://www.fluidmechanics.tudelft.nl/sw Copyright (c) 2006 Delft University of Technology. Permission is granted to copy, distribute and/or modify this document under the terms of the GNU Free Documentation License, Version 1.2 or any later version published by the Free Software Foundation; with no Invariant Sec- tions, no Front-Cover Texts, and no Back-Cover Texts. A copy of the license is available at http://www.gnu.org/licenses/fdl.html#TOC1http://www.gnu.org/licenses/fdl.html#TOC1. Contents 1 Introduction 1 1.1 Historicalbackground. 1 1.2 Purposeandmotivation . 2 1.3 Readership............................. 3 1.4 Scopeofthisdocument. 3 1.5 Overview.............................. 4 1.6 Acknowledgements ........................ 5 2 Governing equations 7 2.1 Spectral description of wind waves . 7 2.2 Propagation of wave energy . 10 2.2.1 Wave kinematics . 10 2.2.2 Spectral action balance equation . 11 2.3 Sourcesandsinks ......................... 12 2.3.1 Generalconcepts . 12 2.3.2 Input by wind (Sin).................... 19 2.3.3 Dissipation of wave energy (Sds)............. 21 2.3.4 Nonlinear wave-wave interactions (Snl) ......... 27 2.4 The influence of ambient current on waves . 33 2.5 Modellingofobstacles . 34 2.6 Wave-inducedset-up . 35 2.7 Modellingofdiffraction. 35 3 Numerical approaches 39 3.1 Introduction........................... -
Surface Waves NOAA Tech Refresh 20 Jan 2012 Kipp Shearman, OSU Outline
Surface Waves NOAA Tech Refresh 20 Jan 2012 Kipp Shearman, OSU Outline – Surface winds • Wind stress • Beaufort scale • Buoy measurements – Surface Gravity Waves • Wave characteristics • Deep/Shallow water waves • Generation • Modeling January mean atmospheric circulation and surface winds Fig 2.3 Ocean Circulation July mean atmospheric circulation and surface winds Fig 2.3 Ocean Circulation Wind Forcing at the Ocean Surface • Wind-forcing can generate currents and waves, as wind transfers some of its momentum into the ocean" •! Wind acts via friction at the surface: wind stress τ# " # # Stresses have units of N/m2, (force/area), like pressure.# Stresses are forces parallel to a surface, pressure is force perpendicular to the surface." •! Force/Area depends on the square of the wind speed u, and it points in the same direction as the wind: " 2 τ ∝ u C drag coefficient 1.4 10−3 " D = ≈ × C u u 3 τ = ρa D density of air 1.3 kg / m " ρa = ≈ Example: 20kt wind $ 10 m/s → 0.18 N/m2 = 1.8 dyne/cm2" 0, <1 knot 1, 1-3 knots 2, 4-6 knots 3, 7-10 knots 4, 11-17 knots 5, 17-21 knots 6, 22-27 knots 7, 28-33 knots 8, 33-40 knots 9, 41-47 knots 10, 48-55 knots 11, 56-63 knots Beaufort scale, after http://www.geology.wmich.edu/Kominz/windwater.html Beaufort scale still provides climatological data Look at buoy winds off oregon coast. http://www.wrh.noaa.gov/pqr/ Outline –! Surface winds •! Wind stress •! Beaufort scale •! Buoy measurements –! Surface Gravity Waves •! Wave characteristics •! Deep/Shallow water waves •! Generation •! Modeling Wave Propagation • Wave Period T: time between arrival of successive wave crests at a given place • Wave Length L: distance between successive wave crests • Wave (phase) speed c: cp = L / T By definition, the definition of cp is valid for all Segar waves.