Lagrangian Measurement of Subsurface Poleward Flow Between 38 Degrees N and 43 Degrees N Along the West Coast of the United States During Summer, 1993

Total Page:16

File Type:pdf, Size:1020Kb

Lagrangian Measurement of Subsurface Poleward Flow Between 38 Degrees N and 43 Degrees N Along the West Coast of the United States During Summer, 1993 CORE Metadata, citation and similar papers at core.ac.uk Provided by Calhoun, Institutional Archive of the Naval Postgraduate School Calhoun: The NPS Institutional Archive Faculty and Researcher Publications Faculty and Researcher Publications 1996-09-01 Lagrangian Measurement of subsurface poleward Flow between 38 degrees N and 43 degrees N along the West Coast of the United States during Summer, 1993 Collins, Curtis A. Geophysical Research Letters, Vol. 23, No. 18, pp. 2461-2464, September 1, 1996 http://hdl.handle.net/10945/45730 GEOPHYSICAL RESEARCH LETTERS, VOL. 23, NO. 18, PAGES 2461-2464, SEPTEMBER 1, 1996 Lagrangian Measurement of subsurface poleward Flow between 38øN and 43øN along the West Coast of the United States during Summer, 1993 CurtisA. Collins,Newell Garfield, Robert G. Paquette,and Everett Carter 1 Departmentof Oceanography,Naval Postgraduate School, Monterey, California Abstract. SubsurfaceLagrangian measurementsat about Undercurrentalong the coastsof California and Oregon. We 140 m showedthat the pathof the CaliforniaUndercurrent lay are using quasi-isobaric(float depth controlled primarily by next to the continentalslope betweenSan Francisco(37.80N) the pressureeffect on density)RAFOS floats (Rossby et al., and St. GeorgeReef (41.8øN) duringmid-summer 1993. The 1986) to make these measurements. A RAFOS float consists meanspeed along this 500 km pathwas 8 cms-1. Theflow at of a hydrophonemounted in a glasstube that is about2 meters this depth was not disturbedby upwelling centersat Point long. These hydrophonesreceive signals from three sound Reyesor CapeMendocino. Restfits also demonstratethe abil- sources that were moored 400 km offshore between 34.3øN and ity to acousticallytrack floats located well above the sound 40.4øN.The sound sources emit 15 W, 80 s signalsa•t 260 Hz channelaxis along the California coast. threetimes per day. The sourcesare mooredat the centerof the SOFARchannel, which occursat depthsranging :from 500 to Introduction 600 m off the California Coast. Beginningthis program,we wereunsure hoW' shallow we The existenceof polewardsubsurface flow along the West . could place the floats. The observeddepth of the maximum Coast of the United States is well known. Along the polewardflow off Central California appearsto be about 150 continentalshelf and upper slope, polewardflow has been m (Rischmiller,1993), so this would be the ideal depth. But observedusing both direct measurements,including current optimum sound propagation, and hence position fixing, meters(e.g., Wickhamet al., 1987, Huyer et al., 1989) and occurs near the depth of the axis of the SOFAR channel. short term drogue deployments(Reid, 1962), and indirect Deploying floats in the SOFAR channel(550 to 600 m) would methods based upon geostrophy (Chelton, 1984). The avoid the "shadow"zones that are createdby fronts associated poleward flow is called the California Undercurrentand with mesoscale features in shallower waters. Our floats have transportsequatorial waters poleward, resulting in a wedgeof beenset at a varietyof depthsin the upperhalf of the SOFAR warm, high salinity and low oxygen water at intermediate channel,from 140 m to 700 m. The purposeof this letteris to depthnext to the coast(Lynn and Simpson,1987). These describethe behaviorof the shallowestfloat, not only because waterscontrast with the equatorwardflowing Subarcticwaters this float trajectorywas similar to that for the deeperfloats that lie offshoreand are relatively cool, fresh and highly thatwere in the Undercurrent,but also becauserobust tracking oxygenated. As pointed out by Mooers (1989), questions remain about the character of the flow in the California at shallow depthsmay allow the use of quasi-isopycnal(or Undercurrent: is the current a continuous flow or a series of pressure-effectcompensated)RAFOS technology to better connected eddies? samplethermodynamic processes associated with upwelling. Barriersto continuoussubsurface alongshore flow are most likely to exist at capes. During summer,upwelling is espe- Results cially persistentand well developedat Pt. Arena and Cape Mendocino(Bray andGreengrove, 1993), and is evidencedby RAFOS float NPS#5 was launchedon July 7, 1993, in the California Undercurrent above the 1000 m isobath due west of minimum sea surface temperature. Instabilities in the alongshoreflow develop, forming filaments and eddies. San Franciscoand surfacedon September5, 1993, about 60 Filamentsof cold water are subsequentlyobserved flowing in km off Cape Blanco, Oregon. During its subsurfacemission, NPS#5 was able to hear at least two of the three offshore sound an offshore direction (sometimesextending for hundredsof kilometers) from these upwelling centers, restilting in the sourcesduring 162 of the 180 listening periods,and all three transportof water from the shelf into the deep ocean(Brink sourceswere heard during 92 of the listeningperiods. Since a and Cowles, 1991). These filaments have offshore-directed minimumof two sourcesis requiredto fix the positionof the velocitiesthat may exceed 50 cms-1 at the surfaceand have float, we were able to constructa trajectoryfor the float. The beenobserved to extendfrom the surfaceto greaterthan 500 m longest period when no or only one sourcewas heard was 18 hours. This occurred four times. off Point Arena (Ramp et al., 1991). We have recently begun a programof Lagrangianmeasure- The trackof the float is indicatedin Figure 1 as a seriesof mentsto study the continuityand structureof the California daily positionsplotted on an advanced very high resolution radiometer(AVHRR) sea surfacetemperature image from a 1NowatTaygeta Scientific Inc.,•Monterey, California NOAA polar-orbiting satellite for September 2, 1993. (Vertical motionof the float is alsoindicated in Figure 1: open Thispaper is not subjectto U.S. copyright.Pub- dots representsinking, while solid dots represent shoaling.) lishedin 1996by theAmerican Geophysical Union. After launch the float first drifted northwestward and then northeastward,turning to the northwestagain upon reaching Papernumber 96GL0213 8 the 200 m isobath. The float remained in the Undercurrent, 2461 2462 COI.I.INS, ET AL: POLEWARD FLOW ALDNG THE U.S. WEST COAST IN SUMMER 1993 I 17.00 I Pt Arena 9. O0 '%. Figure1. Chartof the trajectoryof RAFOSfloat NPS#5. The trajectorybegins off SanFrancisco at 37'-50.4'N, 123'-27.3'W on July 7, 1993, andends just southof CapeBlanco at 42ø-43.6'N, 125ø-06.4'Won September5, 1993. Positionsare indicatedby circlesand are given daily. Open (closed)circles indicate regions where the float sinks (rises). Isothermsare derived from AVHRR imageryfor September2, 1993. movingsteadily poleward with a meanspeed of 8 cms-1, along these locationson these dates was confirmed by examination the 200 m isobath. During this polewarddrift, the float passed of AVHRR imagery.) After passingto the west of St. George tradertwo major upwelling centers: Pt. Arena on July 18 and Reef at 41.80N on August 10, the float drifted offshore into Cape Mendocinoon July 28. (The existenceof upwellingat water 4000 m deep in the Gorda basin. Here it became COl J!.INS, ET AL.: POLEWARD FLOW ALONG THE U.S. WEST COAST IN SUMMER 1993 2463 entrainedin an anticycloniceddy, moving around the eddy Three regions of shoaling(the float encounteringdenser three times with a circular motion of 35 km diameter. During water) were observed: from just north of Pt. Reyes to Pt. its third circuitaround the eddy,NPS#5 was displacedfarther to Arena, a midway betweenCape Mendocino and St. George the westand north. The trajectoryends with the surfacingof Reef, and during the northwardand westwardflow from just the float on September5, 1995. south of St. George Reef to 125.2øW. Sinking occurred The speed of the float is proportionalto the distance before, betweenand after theseperiods. At Point Arena and betweenthe daily positionsgiven in Figure 1, i.e., the faster CapeMendocino, minimum pressurewas observedjust to the the float movesthe greaterthe distancebetween the positions. southof the Point/Cape,while off St. George Reef minimum (The distance between the daily positions is actually the pressurewas observedoffshore as the float crossed42øN. Each minimum distance that the float moves, because small me- of these positionscoincided with the general location of an anders,tidal motions, etc. cause small deviations along this upwelling center as defined by temperatureminima in the path). Along the coast,minimum speedsoccur at Pt. Reyes, AVHRR image(Figure 1). While the float was entrainedin the just to the southof Pt. Arena and St. GeorgeReef, and just to anticycloniceddy off Cape Blanco, the float rose as it moved the north of Cape Mendocino. The largestspeeds, 15 to 20 offshore and sank as it moved toward the coast. At the end of cms-1, occurred during offshore movement north of St. George its mission,the float was about20 decibarsdeeper than when Reef,while along the coastspeeds greater than 10 cms4 it was launched. occurredjust to the north of Pt. Reyes,just south of Cape Within the regionshown in Figure 1, temperaturegenerally Mendocino, and about halfway betweenPt. Arena and Cape decreasesto the north, inshore(during summer,due to up- Mendocino. welling) and with increasingpressure (a typical CTD cast The float also measuredpressure and temperatureduring its showstemperature decreases with increasingpressure at -0.01 mission,which is shownin Figure 2. The pressureof the float to -0.02øCdbar4 at 140 dbar). The float cooledboth as it variedfrom 160 decibars (dbar, I dbar= 104Pa~ 1 m)
Recommended publications
  • Ebb and Flow Tides and Life on Our Once and Future Planet
    This article has This been published in or collective redistirbution of any portion of this article by photocopy machine, reposting, or other means is permitted only with the approval of The approval portionthe ofwith any permitted articleonly photocopy by is machine, of this reposting, means or collective or other redistirbution BOOK REVIEWS Ebb and Flow Oceanography Tides and Life on Our Once and Future Planet , V By Tom Koppel, The Dundurn Group, which is the loss of much of the fleet of olume 21, Number 2, a quarterly journal of journal The olume 21, Number 2, a quarterly 2007, 296 pages, ISBN 9781550027266, Alexander the Great due to a tidal bore), Paperback, $26.99 US coastal ecosystems, modern analysis, and extracting energy from tides. Chapter 1 REVIEWED BY JOHN L. LuiCK contains an account of the ancient tidal dockyards at Lothal, India—surely a can- Ebb and Flow: Tides and Life on Our didate for “Engineering Wonders of the Once and Future Planet is well titled. It Ancient World.” The most ambitious and O tells the story of tides, why they matter, original chapter is the final one, whose ceanography Society. Society. ceanography what causes them, and how they have three subheadings are Sea Level Change changed over time. The author, Tom Causes Intertidal Zones to Migrate; Giant all sorts of ammonia and phosphoric Koppel, is not an analyst or theoretician Ancient Tides and Earth’s Rotation; and salts.” Again, tides are shown to play a C of tides but a man of inquisitive mind The Origin, Evolution, and Future of Life crucial role in both the origin and the opyright 2008 by The 2008 by opyright and substantial beachcombing and on Earth.
    [Show full text]
  • The Evolution and Demise of North Brazil Current Rings*
    VOLUME 36 JOURNAL OF PHYSICAL OCEANOGRAPHY JULY 2006 The Evolution and Demise of North Brazil Current Rings* DAVID M. FRATANTONI Department of Physical Oceanography, Woods Hole Oceanographic Institution, Woods Hole, Massachusetts PHILIP L. RICHARDSON Department of Physical Oceanography, Woods Hole Oceeanographic Institution, and Associated Scientists at Woods Hole, Woods Hole, Massachusetts (Manuscript received 27 May 2004, in final form 26 October 2005) ABSTRACT Subsurface float and surface drifter observations illustrate the structure, evolution, and eventual demise of 10 North Brazil Current (NBC) rings as they approached and collided with the Lesser Antilles in the western tropical Atlantic Ocean. Upon encountering the shoaling topography east of the Lesser Antilles, most of the rings were deflected abruptly northward and several were observed to completely engulf the island of Barbados. The near-surface and subthermocline layers of two rings were observed to cleave or separate upon encountering shoaling bathymetry between Tobago and Barbados, with the resulting por- tions each retaining an independent and coherent ringlike vortical circulation. Surface drifters and shallow (250 m) subsurface floats that looped within NBC rings were more likely to enter the Caribbean through the passages of the Lesser Antilles than were deeper (500 or 900 m) floats, indicating that the regional bathymetry preferentially inhibits transport of intermediate-depth ring components. No evidence was found for the wholesale passage of rings through the island chain. 1. Introduction ration from the NBC, anticyclonic rings with azimuthal speeds approaching 100 cm sϪ1 move northwestward a. Background toward the Caribbean Sea on a course parallel to the The North Brazil Current (NBC) is an intense west- South American coastline (Johns et al.
    [Show full text]
  • University Microfilms, Inc., Ann Arbor, Michigan the SYNTHESIS of POINT DATA
    This dissertation has been microfilmed exactly as received 68-16,949 JOHNSON, Rockne Hart, 1930- THE SYNTHESIS OF POINT DATA AND PATH DATA IN ESTIMATING SOFAR SPEED. University of Hawaii, Ph.D., 1968 Geophysics University Microfilms, Inc., Ann Arbor, Michigan THE SYNTHESIS OF POINT DATA AND PATH DATA IN ESTIMATING SOFAR SPEED A DISSERTATION SUBMITTED TO THE GRADUATE DIVISION OF THE UNIVERSITY OF HAWAII IN PARTIAL FULFILLMENT OF THE REQUIREMENTS FOR THE DEGREE OF DOCTOR OF PHILOSOPHY IN GEOSCIENCES June 1968 By Rockne Hart Johnson Dissertation Committee: William M. Adams, Chairman Doak C. Cox George H. Sutton George P. Woollard Klaus Wyrtki ii P~F~E Geophysical interest in the deep ocean sound (sofar) channel centers on its use as a tool for the detection and location of remote events. Its potential application to oceanography may lie in the monitoring of variations of physical properties averaged over long paths by sofar travel-time measurements. As the accuracy of computed event locations is generally dependent on the accuracy of travel-time calculations, the spatial and temporal variation of sofar speed is a matter of fundamental interest. The author's interest in this problem has grown out of a practical need for such information for application to the problem of locating the sources of earthquake I waves and submarine volcanic sounds. Although an exten­ sive body of sound-speed data is available from hydrographic casts, considerably more precise measurements can be made of explosion travel times over long paths. This dissertation develops a novel procedure for analytically combining these two types of data to produce a functional description of the spatial variation of safar speed.
    [Show full text]
  • Overview of the Impacts of Anthropogenic Underwater Sound in the Marine Environment
    Overview of the impacts of anthropogenic underwater sound in the marine environment Biodiversity Series 2009 Overview of the impacts of anthropogenic underwater sound in the marine environment OSPAR Convention Convention OSPAR The Convention for the Protection of the La Convention pour la protection du milieu Marine Environment of the North-East Atlantic marin de l'Atlantique du Nord-Est, dite (the “OSPAR Convention”) was opened for Convention OSPAR, a été ouverte à la signature at the Ministerial Meeting of the signature à la réunion ministérielle des former Oslo and Paris Commissions in Paris anciennes Commissions d'Oslo et de Paris, on 22 September 1992. The Convention à Paris le 22 septembre 1992. La Convention entered into force on 25 March 1998. It has est entrée en vigueur le 25 mars 1998. been ratified by Belgium, Denmark, Finland, La Convention a été ratifiée par l'Allemagne, France, Germany, Iceland, Ireland, la Belgique, le Danemark, la Finlande, Luxembourg, Netherlands, Norway, Portugal, la France, l’Irlande, l’Islande, le Luxembourg, Sweden, Switzerland and the United Kingdom la Norvège, les Pays-Bas, le Portugal, and approved by the European Community le Royaume-Uni de Grande Bretagne and Spain. et d’Irlande du Nord, la Suède et la Suisse et approuvée par la Communauté européenne et l’Espagne. 2 OSPAR Commission, 2009 Acknowledgements Author list (in alphabetical order) Thomas Götz Scottish Oceans Institute, East Sands University of St Andrews St Andrews, Fife KY16 8LB [email protected] Module 2, 8 Gordon Hastie SMRU Limited New Technology Centre North Haugh St Andrews, Fife KY16 9SR [email protected] Module 2, 8 Leila T.
    [Show full text]
  • Particle Pathways in the Gulf Stream
    Particle Pathways and P-T Shaw2 in the Gulf Stream Abstract East of Cape Hatteras, the Gulf Stream front separates two water masses: Sargasso Sea water to the south and the An experiment is under way to study the kinematics, dynamics, and cold slope waters to its north. The sharpness of the water mass path evolution of the Gulf Stream front between Cape Hatteras and boundary along the current's cyclonic edge and its coincidence 60°W. The Rafos float, which can track the true motion of water with the stream suggests that the front is impermeable to parcels along density surfaces which slope steeply across the Gulf Stream, has recently been developed for this study. These instruments cross-stream exchange of water. (It should be noted that this are launched in the center of the Gulf Stream every 5-15 days for a distinction of separate water masses loses validity below the 30-day mission. Each float provides a trajectory and a continuous midthermocline, where increasing uniformity of water prop- record of temperature and pressure along the trajectory. Our results erties suggests greater cross-stream exchange.) The Gulf so far show that: a) cross-stream motion has a significant vertical -1 Stream is not so isolated from the Sargasso Sea, however. Be- component (ranging to some 0.1 cm • s ) compared to vertical veloc- ities in midocean; b) floats systematically shoal (upwell) as they ap- tween the Florida Straits and Cape Hatteras the transport of proach anticyclonic meanders and deepen (downwell) as they ap- water more than doubles, with nearly all the new water coming proach cyclonic meanders; c) more than half of the floats launched from the Sargasso Sea.
    [Show full text]
  • Acceleration in Acoustic Wave Propagation Modelling Using Openacc/Openmp and Its Hybrid for the Global Monitoring System
    Acceleration in Acoustic Wave Propagation Modelling using OpenACC/OpenMP and its hybrid for the Global Monitoring System Noriyuki Kushida*1, Ying-Tsong Lin*2, Peter Nielsen*1, and Ronan Le Bras*1 *1 CTBTO Preparatory Commission for the Comprehensive Nuclear-Test-Ban Treaty Organization Provisional Technical Secretariat *2 Woods Hole Oceanographic Institution, USA Disclaimer: The views expressed herein are those of the author(s) and do not necessarily reflect the views of the CTBT Preparatory Commission. Background (Who we are) The CTBT (Comprehensive Nuclear-Test-Ban Treaty) bans all types of nuclear explosions. CTBTO operates a worldwide monitoring system to catch the signs of nuclear explosions with four technologies: Seismic Infrasound Hydroacoustic Radionuclide Atmospheric explosion Underground explosion Underwater explosion 2 Background (Underwater event and Hydroacoustic observation) ● Hydroacoustic: acoustic waves through the Ocean Seismometer Hydrophone Phase conversion Underwater explosion ● A big explosion in the Ocean can generate a sound wave ● We can catch such sounds with ○ microphones in the Ocean (hydrophone) ○ seismometers on the coast Photo/Video from CTBTO Website Background (Hydroacoustic stations in CTBTO) ● “H” icone: Hydrophone (H-phase). 6 stations ● “T” icone: Seismometer (T-phase). 4 stations ● Hydroacoustic waves can travel very long distances ○ Complex phenomena can be involved ● Seismic stations; 170 (50 primary + 120 auxiliary) to cover the globe An example: Argentinian submarine ARA San Juan 1/3 Last Contact
    [Show full text]
  • Characteristics of Intermediate Water Flow in the Benguela Current As
    Deep-Sea Research II 50 (2003) 87–118 Characteristics of intermediate water flow in the Benguela current as measured with RAFOS floats P.L. Richardsona,*, S.L. Garzolib a Department of Physical Oceanography, Woods Hole Oceanographic Institution, 360 Woods Hole Road, Woods Hole, MA 02543, 3 Water Street, P.O. Box 721, USA b Atlantic Oceanographic and Meteorological Laboratory, NOAA, 4301 Rickenbacker Causeway, Miami, FL 33149, USA Received 28 September 2001; accepted 26 July 2002 Abstract Seven floats (not launched in rings) crossed over the mid-Atlantic Ridge in the Benguela extension with a mean westward velocity of around 2 cm=s between 22S and 35S. Two Agulhas rings crossed over the mid-Atlantic Ridge with a mean velocity of 5:7cm=s toward 2851: This implies they translated at around 3:8cm=s through the background velocity field near 750 m: The boundaries of the Benguela Current extension were clearly defined from the observations. At 750 m the Benguela extension was bounded on the south by 35S and the north by an eastward current located between 18S and 21S. Other recent float measurements suggest that this eastward current originates near the Trindade Ridge close to the western boundary and extends across most of the South Atlantic, limiting the Benguela extension from flowing north of around 20S. The westward transport of the Benguela extension was estimated to be 15 Sv by integrating the mean westward velocities from 22S to 35S and multiplying by the 500 m estimated thickness of intermediate water. Roughly 1.5 Sv of this are transported by the B3 Agulhas rings that cross the mid-Atlantic Ridge each year (as observed with altimetry).
    [Show full text]
  • Oceanography
    Oceanography Course Outline Unit One Introduction to Oceanography 7 days Unit Two Structure of the Earth & Modern Navigational Techniques 7 days Unit Three Plate Tectonics 7 days Unit Four The Sea Floor and Its Sediments 9 days Unit Five Physical and Chemical Properties of Water 7 days Unit Six The Atmosphere and Circulation 5 days Unit Seven Ocean Structure and Currents 7 days Unit Eight Waves 5 days Unit Nine Tides 5 days Unit Ten Coasts, Beaches & Estuaries 12 days Unit Eleven Marine Biology 14 days School-wide Academic Expectations Addressed in Oceanography: Problem Solving Critical Thinking Collaboration Writing Skills School-wide Social and Civic Expectations Addressed in Oceanography: Honesty Responsibility Respect Safety Common Core Standards Addressed in Oceanography: Reading Standard for Science Literacy (RST): 2, 3, 4, 7, 8, 9 Writing Standards for Science Literacy (WHST): 1, 2, 4, 9 NGSS Standards Addressed in Oceanography: TBD Unit 1: Introduction to Oceanography Introduction: Oceanography is a multidisciplinary field in which geology, chemistry, physics, and biology are incorporated. This unit focuses on the historical perspective - the contributions of various individuals/groups and the advancement of technology in the development of our understanding of the oceans. CT State Standard(s): Energy in the Earth System. Common Core Standard(s): · Reading Standard for Science Literacy (RST): 2, 3, 4, 7, 8, 9 · Writing Standards for Science Literacy (WHST): 1, 2, 4, 9 School-wide Academic Expectations Addresses in this
    [Show full text]
  • WILLIAM MAURICE EWING May 12, 1906-May 4, 1974
    NATIONAL ACADEMY OF SCIENCES WILLIAM MAURICE Ew ING 1906—1974 A Biographical Memoir by ED W A R D C . B ULLARD Any opinions expressed in this memoir are those of the author(s) and do not necessarily reflect the views of the National Academy of Sciences. Biographical Memoir COPYRIGHT 1980 NATIONAL ACADEMY OF SCIENCES WASHINGTON D.C. WILLIAM MAURICE EWING May 12, 1906-May 4, 1974 BY EDWARD C. BULLARD* CHILDHOOD, 1906-1922 ILLIAM MAURICE EWING was born on May 12, 1906 in W Lockney, a town of about 1,200 inhabitants in the Texas panhandle. He rarely used the name William and was always known as Maurice. His paternal great-grandparents moved from Kentucky to Livingston County, Missouri, at some date before 1850. Their son John Andrew Ewing, Maurice's grandfather, fought for the Confederacy in the Civil War; while in the army he met two brothers whose family had also come from Kentucky to Missouri before 1850 and were living in De Kalb County. Shortly after the war he married their sister Martha Ann Robinson. Their son Floyd Ford Ewing, Maurice's father, was born in Clarkdale, Mis- souri, in 1879. In 1889 the family followed the pattern of the times and moved west to Lockney, Texas. Floyd Ewing was a gentle, handsome man with a liking for literature and music, whom fate had cast in the unsuitable roles of cowhand, dryland farmer, and dealer in hardware and farm implements. Since he kept his farm through the *This memoir is a corrected and slightly amplified version of one published by the Royal Society in their Biographical Memoirs (21:269-311, 1975).
    [Show full text]
  • Long-Term Autonomous Hydrophones for Large-Scale Hydroacoustic Monitoring of the Oceans Jean-François D’Eu, Jean-Yves Royer, Julie Perrot
    Long-term autonomous hydrophones for large-scale hydroacoustic monitoring of the oceans Jean-François d’Eu, Jean-Yves Royer, Julie Perrot To cite this version: Jean-François d’Eu, Jean-Yves Royer, Julie Perrot. Long-term autonomous hydrophones for large- scale hydroacoustic monitoring of the oceans. Yeosu 2012, May 2012, Yeosu, North Korea. pp.1-6, 10.1109/OCEANS-Yeosu.2012.6263519. insu-00817948 HAL Id: insu-00817948 https://hal-insu.archives-ouvertes.fr/insu-00817948 Submitted on 22 May 2019 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. Long-term autonomous hydrophones for large-scale hydroacoustic monitoring of the oceans Jean-François D’Eu, Jean-Yves Royer, Julie Perrot Laboratoire Domaines Océaniques CNRS and University of Brest Plouzané, France [email protected] Abstract—We have developed a set of long-term autonomous hydrophones dedicated to long-term monitoring of low-frequency A. Monitoring ocean seismicity at a broad scale sounds in the ocean (<120Hz). Deploying arrays of such Seismicity in the ocean is usually recorded with the help of hydrophones (at least 4 instruments) proves a very efficient seismometers, such as Ocean Bottom Seismometers (OBS), approach to monitor acoustic events of geological origin placed in the proximity of active areas.
    [Show full text]
  • Sound Speed in the Mediterranean Sea: an Analysis from a Climatological Data Set
    c Annales Geophysicae (2003) 21: 833–846 European Geosciences Union 2003 Annales Geophysicae Sound speed in the Mediterranean Sea: an analysis from a climatological data set S. Salon1, A. Crise1, P. Picco2, E. de Marinis3, and O. Gasparini3 1Istituto Nazionale di Oceanografia e di Geofisica Sperimentale–OGS, Borgo Grotta Gigante 42/C, I-34010 Sgonico–Trieste, Italy 2Centro Ricerche Ambiente Marino, CRAM-ENEA, S.Teresa, Localita` Pozzuolo di Lerici, I-19100, La Spezia, Italy 3DUNE s.r.l., Via Tracia 4, I-00183 Roma, Italy Received: 9 April 2002 – Revised: 26 August 2002 – Accepted: 18 September 2002 Abstract. This paper presents an analysis of sound speed served in the northwestern Mediterranean (Send et al., 1995) distribution in the Mediterranean Sea based on climatologi- and in the Greenland Sea (Pawlowicz et al., 1995; Morawitz cal temperature and salinity data. In the upper layers, prop- et al., 1996). Ocean acoustic tomography has also proved to agation is characterised by upward refraction in winter and be a methodology for the observation of currents and internal an acoustic channel in summer. The seasonal cycle of the tides (Shang and Wang, 1994; Demoulin et al., 1997). These Mediterranean and the presence of gyres and fronts create a successful applications propose ocean tomography as a tool wide range of spatial and temporal variabilities, with rele- for large-scale monitoring of the oceans in the frame of the vant differences between the western and eastern basins. It development of Global Oceans Observing Systems (GOOS). is shown that the analysis of a climatological data set can In spite of this growing interest in acoustic inversion, an help in defining regions suitable for successful monitoring by analysis of the sound speed field in the Mediterranean Sea is means of acoustic tomography.
    [Show full text]
  • Underwater Acoustics - Gee-Pinn James Too
    OCEANOGRAPHY – Vol.III - Underwater Acoustics - Gee-Pinn James Too UNDERWATER ACOUSTICS Gee-Pinn James Too National Cheng Kung University, Taiwan Keywords: Underwater Acoustics, Underwater Communication, Underwater Detection, Sound Velocity Profiles, Surface Duct, Shadow Zone, SOFAR (Deep Sea) Channel, Acoustic Ray Model, Normal Mode Model, PE (Parabolic Wave Equation) Models, Temperature, Pressure, and Salinity. Contents 1. An Acoustical View of Oceanography 2. The History of Research on Ocean Acoustics 3. Measurement of Speed of Sound 3.1. The Sound Speed Profile 3.2. Propagation Theory 3.3. Applications of Underwater Acoustics 4. Other Applications Bibliography Biographical Sketch Summary Underwater acoustics is an important science with significant practical application, especially for the application in ocean. Electro-magnetic waves, which are strongly absorbed by water, have their limits in propagation range in water. Therefore, acoustic waves play an important role on the navigation, underwater communication, underwater detection, and investigation in ocean research. The ocean is an inhomogeneous medium with various sound velocity profiles that vary with depth because of changes in temperature, hydrostatic pressure and salinity. Due to these sound velocity profiles, acoustic wave propagation in ocean results in several interesting phenomena such as surface duct, shadow zone, SOFAR (deep sea) channel, etc. These phenomena all have practical application in underwater communication and detection. Theoretical models and their numerical algorithms for wave propagation are developedUNESCO to describe the complicated ocean– phenomenaEOLSS of wave propagation. Some of these models, such as: acoustic ray model, normal mode model, PE (parabolic wave equation) models are described in this section. SAMPLE CHAPTERS Sonar equations comprise a group of parameters, which considers the phenomena and effects of the underwater sound.
    [Show full text]