DOCSLIB.ORG

Jurassic Guyots on the Southern Iberian Continental Margin: a Model of Isolated Carbonate Platforms on Volcanic Submarine Edifices J

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Jurassic Guyots on the Southern Iberian Continental Margin: a Model of Isolated Carbonate Platforms on Volcanic Submarine Edifices J Jurassic guyots on the Southern Iberian Continental Margin: a model of isolated carbonate platforms on volcanic submarine edifices J. A. Vera*1 J. M. Molina2 P. Montero3 and F. Bea3 1Departamento de EstratigrafõÂa y PalaeontologõÂa, Universidad de Granada, 18071 Granada, Spain; 2Departamento de GeologõÂa, Universidad de JaeÂn, 23071 JaeÂn, Spain; 3Departamento de MineralogõÂa y PetrologõÂa, Universidad de Granada, 18071 Granada, Spain ABSTRACT During the middle Jurassic on the Southern Iberian Continental megasequence (Bajocian±Bathonian) with hummocky cross- Margin (at the westernmost end of the northern Tethys) isolated stratification strata below oolitic shoals, shows that very carbonate platforms developed over volcanic edifices, forming shallow isolated carbonate platforms developed above the guyots. The volcanic edifices were composed of K-rich pillow- volcanic edifices, with similar facies to those recognized in lavas and pyroclastic rocks with a radiometric age & 170 Myr. other guyots, but with a different age and geodynamic context. Such phenomena have not been described until now in this continental margin nor in other passive continental margins of Terra Nova, 9, 163±166, 1997 Alpine domains. The presence of a shallowing-upward part of the tilted fault blocks (Vera et same biozone, to groups of superim- Introduction al., 1988). posed flows some hundreds of metres The Betic Cordillera (Southern Spain) Jurassic submarine volcanic rocks thick with interbedded sedimentary rocks is the westernmost European Alpine (JSVR) have been studied by various from different stages. In the time inter- chain. The External Zones of this Cor- authors (Portugal et al., 1995, and pre- val and areas studied, the total thick- dillera (Prebetic and Subbetic) are com- vious works cited therein) who, in their ness of the volcanic rocks is over 300 m posed mainly of sedimentary rocks, more recent papers, consider them (Fig. 1d). The area chosen for this study deposited from the Triassic to the early transitional-alkaline, originating in an (Alicu n de Ortega) has excellent JSVR Miocene in the Southern Iberian Con- extensional process of crustal thinning. outcrops, where surface alteration of tinental Margin. The Subbetic corre- The main aim of this work is to the volcanic rocks is low. We have sponds to the part of this margin in describe shallow marine materials over analys ed two sets of samples (Al and which pelagic facies from the early the Jurassic volcanic edifices of this V in Fig. 1d), attempting to establish Pliensbachian dominated, when a rift- margin. Our data indicate that the edi- radiometric dating with Rb/Sr in each, ing phase began, with the initial devel- fices were guyots. We use the term guyot the first in the lower lava flows (samples opment of a passive continental margin in the sense of the Glossary of Geology V-1 to V-12) and the second in the that later evolved into an active margin (Bates and Jackson, 1987) as `a type of higher ones (samples AL-1 to Al-12). and terminated in a continental colli- seamount that has a platform top' and sion with the Internal Zones, originat- is therefore not necessarily located on Geochemical results and ing the Cordillera during the Burdiga- oceanic crust. The main characteristic interpretation lian (Garcõ a-Herna ndez et al., 1980; of the guyots, their flat-topped features Vera, 1988). with summits hundreds of metres below The composition of the AL samples are In the palinspastic reconstruction of water-level, has been interpreted as the ultrapotassic while the second set of the Southern Iberian Margin during result of erosional truncation in volcanic samples (V-1 to V-12) have shoshonitic the middle and late Jurassic, four pa- islands, although some authors have affinities (Vera et al., unpubl. data). To laeogeographical domains can be dif- suggested a primary constructional ori- discuss a petrogenetic model for these ferentiated in the Subbetic, that were gin (Bonatti and Tazieff, 1970). rocks is beyond the scope of this paper, elongated parallel to the margin itself but their chemistry clearly points to (Fig. 1). Jurassic volcanism, mainly a specific geodynamic environment. Volcanism in the Subbetic represented by pillow-lavas interca- Shreyer et al. (1987) proposed that lated between pelagic sediments, ap- similar rocks formed as a consequence Geological and palaeogeographical peared only in the Median Subbetic of KMg-rich fluids released during the settings (Fig. 1). In the Subbetic pelagic sedi- transformation of the assemblage, K- ments of the middle and late Jurassic The JSVR in the Median Subbetic feldspar-biotite, in the presence of ex- have been described sedimentary fea- crops out WSW±ENE in a strip 5±10 cess water to phengite + quartz, which tures against the attribution of great km wide and 250 km long. Basalts with occurs when crustal rocks of suitable depth in the deposition (Molina et al., pillow-lava flows dominate and are in- composition are subducted to a depth 1997) admitting the occurrence of local terbedded with pyroclastic rocks. The of 50±70 km. The reaction of these and temporal emersions of the higher thickness of the volcanic rocks and the fluids with the surrounding mantle first time interval represented by them produces metasomatism and then, when change locally from flows a few metres the geodynamic regime allows, partial *Correspondence: E-mail: [email protected] thick in sedimentary rocks from the melting and segregation of K-rich #1997 Blackwell Science Ltd 163 Ahed Fig marker Bhed Table marker Paper 129 Disc Ched Ref end Dhed Ref start Ref marker Jurassic guyots±isolated carbonate platforms . J.A. Vera et al. Terra Nova, Vol 9, No. 4, 163±166 ............................................................................................................................................................................................................................................. melts. In our case, this idea also finds support from strontium isotope data. On the 87Sr/86Sr vs. 87Rb/86Sr dia- gram, rocks from the V-1 to V-12 set fit the 170 Myr old reference isochron reasonably well, but not the AL set (Fig. 2), which has higher 87Sr/86Sr values. The different dispersion and departure from the reference isochron displayed by both rock series cannot be attributed to post consolidation phe- a nomena, since both rock types are equally affected by them, but alterna- tively they most likely reflect primary differences. The fact that ultrapotassic lavas also have a high proportion of radiogenic strontium could indicate a higher contribution of crustal compo- nent in the form of KMg fluids. Based b on their age relationships, chemistry and isotope geology, we therefore sug- gest that the JSVR originated during the beginning of an extensional regime c in a zone with a thick continental crust, probably overthickenned during the Hercynian convergence. Shallowing-upward megasequence related to volcanic rocks Three types of facies associations (FA) can be differentiated in the sedimentary rocks interbedded between the volcanic rocks and those located on the volcanic edifices. FA1 This is very frequent in the lower sedimentary intercalations. It com- prises pelagic marl/limestone rhythmite with ammonites (Toxamblyites and Skirroceras genera) belonging to the higher part of the early Bajocian. Mud- stone and bioclastic (mainly `filaments') and peloidal wackestone-packstone dominate. In some beds slumps, intra- formational breccias and soft deforma- tion structures occur. They are depos- ited clearly below the storm wave base, with episodes of tectonic instability. FA2 This appears mainly in the med- d ian sedimentary intercalations and is composed of marl/limestone rhythmite Fig. 1 (a) Palaeogeographical reconstruction of the Western Mediterranean area during with some strata of calcisiltites with the Middle Jurassic (after Garcõ a-Herna ndez et al., 1989, modified), with indication of hummocky cross-stratification (HCS) the location of the palinspastic reconstruction cross-section in (b) and (c). Key: 1, and symmetrical wave ripples. Parallel Prebetic; 2±5, Subbetic (2, Intermediate Domain; 3, External Subbetic; 4, Median laminations, marked by alternative pe- Subbetic; 5, Internal Subbetic). 6, Area with minimum thickness of continental crust, in loidal and bioclastic laminae, are also which oceanic crust appeared during the Late Jurassic. (b)±(c), Palinspastic reconstruc- frequent. Nodular and bedded chert tions of the Southern Iberian Continental Margin (b), Middle Toarcian; (c), Upper frequently appear in these calcisiltite Bajocian-Bathonian); (d), Stratigraphic section in the guyot of the Alicu n de Ortega beds, just as described Molina et al. area. (1997) in analogous facies. The occur- 164 #1997 Blackwell Science Ltd Paper 129 Disc Terra Nova, Vol 9, No. 4, 163±166 Jurassic guyots±isolated carbonate platforms . J.A. Vera et al. ............................................................................................................................................................................................................................................. There are several shallowing-upward sediments were deposited in isolated cycles 2±5 m thick, with peloidal wack- platforms located over the volcanic edi- estone in the lower part changing gra- fices, several kilometres wide, that were dually in the upper part to oolitic grain- later covered by younger pelagic sedi- stone, showing shoaling cycles with ments. These isolated carbonate plat-
Load more

Recommended publications
  • Mantle Hydration and Cl-Rich Fluids in the Subduction Forearc Bruno Reynard1,2
    Reynard Progress in Earth and Planetary Science (2016) 3:9 Progress in Earth and DOI 10.1186/s40645-016-0090-9 Planetary Science REVIEW Open Access Mantle hydration and Cl-rich fluids in the subduction forearc Bruno Reynard1,2 Abstract In the forearc region, aqueous fluids are released from the subducting slab at a rate depending on its thermal state. Escaping fluids tend to rise vertically unless they meet permeability barriers such as the deformed plate interface or the Moho of the overriding plate. Channeling of fluids along the plate interface and Moho may result in fluid overpressure in the oceanic crust, precipitation of quartz from fluids, and low Poisson ratio areas associated with tremors. Above the subducting plate, the forearc mantle wedge is the place of intense reactions between dehydration fluids from the subducting slab and ultramafic rocks leading to extensive serpentinization. The plate interface is mechanically decoupled, most likely in relation to serpentinization, thereby isolating the forearc mantle wedge from convection as a cold, potentially serpentinized and buoyant, body. Geophysical studies are unique probes to the interactions between fluids and rocks in the forearc mantle, and experimental constrains on rock properties allow inferring fluid migration and fluid-rock reactions from geophysical data. Seismic velocities reveal a high degree of serpentinization of the forearc mantle in hot subduction zones, and little serpentinization in the coldest subduction zones because the warmer the subduction zone, the higher the amount of water released by dehydration of hydrothermally altered oceanic lithosphere. Interpretation of seismic data from petrophysical constrain is limited by complex effects due to anisotropy that needs to be assessed both in the analysis and interpretation of seismic data.
    [Show full text]
  • Physiography of the Seafloor Hypsometric Curve for Earth’S Solid Surface
    OCN 201 Physiography of the Seafloor Hypsometric Curve for Earth’s solid surface Note histogram Hypsometric curve of Earth shows two modes. Hypsometric curve of Venus shows only one! Why? Ocean Depth vs. Height of the Land Why do we have dry land? • Solid surface of Earth is Hypsometric curve dominated by two levels: – Land with a mean elevation of +840 m = 0.5 mi. (29% of Earth surface area). – Ocean floor with mean depth of -3800 m = 2.4 mi. (71% of Earth surface area). If Earth were smooth, depth of oceans would be 2450 m = 1.5 mi. over the entire globe! Origin of Continents and Oceans • Crust is formed by differentiation from mantle. • A small fraction of mantle melts. • Melt has a different composition from mantle. • Melt rises to form crust, of two types: 1) Oceanic 2) Continental Two Types of Crust on Earth • Oceanic Crust – About 6 km thick – Density is 2.9 g/cm3 – Bulk composition: basalt (Hawaiian islands are made of basalt.) • Continental Crust – About 35 km thick – Density is 2.7 g/cm3 – Bulk composition: andesite Concept of Isostasy: I If I drop a several blocks of wood into a bucket of water, which block will float higher? A. A thick block made of dense wood (koa or oak) B. A thin block made of light wood (balsa or pine) C. A thick block made of light wood (balsa or pine) D. A thin block made of dense wood (koa or oak) Concept of Isostasy: II • Derived from Greek: – Iso equal – Stasia standing • Density and thickness of a body determine how high it will float (and how deep it will sink).
    [Show full text]
  • The Nature of the Mohorovicic Discontinuity, a Compromise 1
    JOURNAL OF GEOPHYSICAL RESEARCH VOL. 68, No. 15 AUGUST 1, 1963 The Nature of the Mohorovicic Discontinuity, A Compromise 1 PETER J. WYLLIE Department of Geochemistry and Minemlogy Pennsylvania State Universit.y, University Park Abstract available . The experimental data and steady-state calculations make it difficult M to explain the discontinuity beneath both oceans and continents on the basis of the same change. The phase oceanic M discontinuity may be a chemical discontinuity between basalt and peridotite , and a similar chemical discontinuity ma,y thus be expected b�neath the conti­ nents. Since ayailable experimental data place the basalt-eclogite phase change at about thE' same depth as the continental M discontinuity, intersections may exist between a zone of chemical discontinuity and a phase transition zone, the transition being either basalt-ecloO"ite or feldspathic peridotite-garnet peridotite. Detection of the latter transition by seismic t�'h­ niques ma,y be difficult. The M discontinuity could therefore represent the basalt-eclogite phase change in some localities (e.g. mountain belts) and the chemical discontinuity in others (e.g. oceans and continental shields). Variations in the depth to the chemical discontinuity and in the positions of geoisotherms produce great flexibility in oro genetic models. Interse;­ tions between the two zones at depth could be reflected at the surface by major fault zones separating large structural blocks of different elevations. Chemical discontinuity. The conyentional termediate between dunite and basalt is view that the Moho discontinuity at the base of qualitatively reasonable for the mantle. the crust is caused by a chemical change from Ringwood [1962a, c] adopted a specific model basaltic rock to peridotite has been expounded compounded from the concepts advanced and recently by Hess [1955], Wager [1958], and developed by many petrologists and geochem­ Harris and Rowell [1960].
    [Show full text]
  • Density of Oceanic Crust
    Density of Oceanic Crust Introduction Procedures Certain properties of a substance are both distinctive and Part 1 relatively easy to determine. Density, the ratio between 1. Complete Report Sheet 1 by calculating the missing a sample’s mass and volume at a specific temperature densities. How will you deal with the differences in and pressure (like standard ambient temperature and significant digits? Make sure to include units in your pressure), is one such property. Regardless of the size of a answers. sample, the density of a substance will always remain the 2. Using the depths and densities from your chart, plot same. The density of a rock sample can, therefore, be used a graph on your own paper (or use an electronic in the identification process. graphing tool) and title it Depth vs. Density. Hint: Think about independent and dependent variables. Using a While density may vary only slightly from rock to rock, blue colored pencil, draw a line of best fit from the XY- detailed sampling and correlation with other factors like intercept through the plotted points. depth may reveal important information about the history of a core, or may help to improve the use of seismic Part 2 profiles. The average density of oceanic crust is 3.0 g/cm3, 1. Find the mass and volume for each of the four continental while continental crust has an average of 2.7 g/cm3. samples as instructed by your teacher. How will you deal with error in the laboratory? How about significant Objectives digits? Record your answers in the space provided.
    [Show full text]
  • Peter Castro | Michael E. Huber
    TEACHER’S MANUAL Marine Science Peter Castro | Michael E. Huber SECOND EDITION Waves and Tides Chapter Introduce the BIG IDEA Waves and Tides Have students watch a short video clip of ocean waves 4 breaking on the shore. Have them make observations about the movement of water as the wave breaks and then retreats back to the ocean. If any students have been to the ocean, have them share their experience of the water and the waves. Pose students these questions and let them discuss responses in small groups. 1. Why does the size of a wave change as it approaches the shore? 2. What factors affect the tides and make the tide come in and leave again? 3. What hardships do marine organisms deal with that live in the intertidal zones? Small groups can share back with the whole group on key GO ONLINE To access points their groups discussed. inquiry and investigative activities to accompany this chapter. Ocean Section Pacing Main Idea and Key Questions Literacy Labs and Activities Standards 4.1 Introduc- 1 day Waves carry energy across the sea surface but Key Questions Activity: tion to Wave do not transport water. Making Waves Energy and 1. What are the three most common generating Motion forces of waves? 2. What are the two restoring forces that cause the water surface to return to its undisturbed state? 4.2 Types of 2 days There are several types of waves, each with its 2.d, 5.j, 6.f, Laboratory Manual: Making Waves own characteristics and different ways of 7.e Waves (p.
    [Show full text]
  • Global Sea Level Rise Scenarios for the United States National Climate Assessment
    Global Sea Level Rise Scenarios for the United States National Climate Assessment December 6, 2012 PhotoPhPhototo prpprovidedrovovidideedd bbyy thtthehe GrGGreaterreaeateter LaLLafourcheafofoururchche PoPortrt CoComommissionmimissssioion NOAA Technical Report OAR CPO-1 GLOBAL SEA LEVEL RISE SCENARIOS FOR THE UNITED STATES NATIONAL CLIMATE ASSESSMENT Climate Program Office (CPO) Silver Spring, MD Climate Program Office Silver Spring, MD December 2012 UNITED STATES NATIONAL OCEANIC AND Office of Oceanic and DEPARTMENT OF COMMERCE ATMOSPHERIC ADMINISTRATION Atmospheric Research Dr. Rebecca Blank Dr. Jane Lubchenco Dr. Robert Dietrick Acting Secretary Undersecretary for Oceans and Assistant Administrator Atmospheres NOTICE from NOAA Mention of a commercial company or product does not constitute an endorsement by NOAA/OAR. Use of information from this publication concerning proprietary products or the tests of such products for publicity or advertising purposes is not authorized. Any opinions, findings, and conclusions or recommendations expressed in this material are those of the authors and do not necessarily reflect the views of the National Oceanic and Atmospheric Administration. Report Team Authors Adam Parris, Lead, National Oceanic and Atmospheric Administration Peter Bromirski, Scripps Institution of Oceanography Virginia Burkett, United States Geological Survey Dan Cayan, Scripps Institution of Oceanography and United States Geological Survey Mary Culver, National Oceanic and Atmospheric Administration John Hall, Department of Defense
    [Show full text]
  • Drilling the Crust at Mid-Ocean Ridges
    or collective redistirbution of any portion of this article by photocopy machine, reposting, or other means is permitted only with the approval of Th e Oceanography Society. Send all correspondence to: [email protected] or Th eOceanography PO Box 1931, Rockville, USA.Society, MD 20849-1931, or e to: [email protected] Oceanography correspondence all Society. Send of Th approval portionthe ofwith any articlepermitted only photocopy by is of machine, reposting, this means or collective or other redistirbution articleis has been published in Th SPECIAL ISSUE FEATURE Oceanography Drilling the Crust Threproduction, Republication, systemmatic research. for this and teaching article copy to use in reserved. e is rights granted All OceanographyPermission Society. by 2007 eCopyright Oceanography Society. journal of Th 20, Number 1, a quarterly , Volume at Mid-Ocean Ridges An “in Depth” perspective BY BENOÎT ILDEFONSE, PETER A. RONA, AND DONNA BLACKMAN In April 1961, 13.5 m of basalts were drilled off Guadalupe In the early 1970s, almost 15 years after the fi rst Mohole Island about 240 km west of Mexico’s Baja California, to- attempt, attendees of a Penrose fi eld conference (Confer- gether with a few hundred meters of Miocene sediments, in ence Participants, 1972) formulated the concept of a layered about 3500 m of water. This fi rst-time exploit, reported by oceanic crust composed of lavas, underlain by sheeted dikes, John Steinbeck for Life magazine, aimed to be the test phase then gabbros (corresponding to the seismic layers 2A, 2B, for the considerably more ambitious Mohole project, whose and 3, respectively), which themselves overlay mantle perido- objective was to drill through the oceanic crust down to tites.
    [Show full text]
  • Cretaceous History of Pacific Basin Guyot Reefs: a Reappraisal Based on Geothermal Endo-Upwelling
    PALAEOZ1c01061 ELSEVIER Palaeogeography, Palaeoclimatology, Palaeoecology 112 (1994) 239-260 Cretaceous history of Pacific Basin guyot reefs: a reappraisal based on geothermal endo-upwelling Francis Rougerie a, J.A. Fagerstrom a QRSTQM, B. P. 529, Papeete, Tahiti, French Polynesia Departinent of GeologicalSciences, The Uiziversity of Colorado, Boulder, CO 80309, USA Received 23 July, 1992; revised and accepted 15 April 1994 Abstract The mid-Cretaceous histories (origin, growth, death) of algal-rudist-stromatoporoid reef communities located on many Pacific Basin guyots are complex and controversial. These shallow water, tropical communities originated on volcanic edifices extruded during the Barremian-Albian, grew upward during edifice subsidenceftransgression throughout the Aptian, Albian and Cenomanian and several of them died almost synchronously near the Cenomanian- Turonian boundary. During their periods of origin and growth, we postulate that the reef ecosystems received dissolved oxygen by wave surge and nutrients by geothermal endo-upwelling. By this process oceanic waters of intermediate depth (approx. 500-1500 m) were: (a) drawn into the weathered and fractured volcanic summit and lower part of the older reef and driven upward through the porous framework by the remnant geothermal gradient of the volcanic foundation and (b) emerged at the reef surface to support the high metabolism of the living community. The death of most of the reefs near the Cenomanian-Turonian boundary approximately coincides with the most intense oceanic anoxic event (Om)in Pacific Ocean history. During this OAE the chemistry of the endo-upwelled fluids arriving at the reef surface changed from nutrient/oxygen-rich to dysoxic-anoxic-toxic, and killed the community.
    [Show full text]
  • Subduction Zones
    SUBDUCTION ZONES Robert J. Stern Geosciences Department University of Texas at Dallas Richardson, Texas, USA Received 24 January 2001; revised 24 June 2002; accepted 11 November 2002; published 31 December 2002. [1] Subduction zones are where sediments, oceanic continental crust, and earthquakes caused by the down- crust, and mantle lithosphere return to and reequilibrate going plate present a growing hazard to society. This with Earth’s mantle. Subduction zones are interior ex- overview summarizes our present understanding of sub- pressions of Earth’s 55,000 km of convergent plate mar- duction zones, using perspectives of the incoming plate, gins and are the geodynamic system that builds island downgoing plate, mantle wedge, and arc-trench com- arcs. Excess density of the mantle lithosphere in subduc- plex. Understanding the operation of subduction zones tion zones provides most of the power needed to move stands as one of the great challenges facing the Earth the plates while inducing convection in the overriding sciences in the 21st century and will require the efforts of mantle wedge. Asthenospheric mantle sucked toward global interdisciplinary teams. INDEX TERMS: 1010 Geochemis- the trench by the sinking slab interacts with water and try: Chemical evolution; 1030 Geochemistry: Geochemical cycles incompatible elements rising from the sinking plate, and (0330); 7299 Seismology: General or miscellaneous; 8120 Tectono- this interaction causes the mantle to melt. These melts physics: Dynamics of lithosphere and mantle—general; 8155 Tectono- rise vertically through downwelling mantle to erupt at physics: Plate motions—general; KEYWORDS: island arc, Wadati-Be- arc volcanoes. Subduction zones are thus interior Earth nioff Zone, subduction, tectonics systems of unparalleled scale and complexity.
    [Show full text]
  • Deep-Ocean Basins
    Chapter23 The Ocean Basins ChapterCh t Outline Outli ne 1 ● The Water Planet Divisions of the Global Ocean Exploration of the Ocean 2 ● Features of the Ocean Floor Continental Margins Deep-Ocean Basins 3 ● Ocean-Floor Sediments Sources of Deep Ocean– Basin Sediments Physical Classification of Sediments Why It Matters Oceans cover more than 70 percent of Earth’s surface. Oceans interact with the atmosphere to influence weather and climate. Exploring and analyzing data about the chemistry of ocean water, the geology of the ocean floor, marine ecosystems, and the physics of water movement is critical to understanding natural processes on Earth. 634 Chapter 23 hhq10sena_obacho.inddq10sena_obacho.indd 663434 PDF 88/1/08/1/08 11:09:46:09:46 PPMM Inquiry Lab 20 min Sink or Float? Fill the bottom half of 3-L soda bottle with water to within about 3 inches from the top and place it on a plastic or metal tray to catch any spills. Using small (3-oz) plastic cups, with some paper clips and metal nuts for ballast, see if you can get a cup to sink with air still trapped inside, simulating a submersible. You may need something pointed to make holes in the cups. Questions to Get You Started 1. What is buoyancy and why is it so important for maritime travel? 2. Compare techniques for sinking the cup. Does one method consistently work better than others? 3. What challenges do engineers face when designing submersibles? 635 hhq10sena_obacho.inddq10sena_obacho.indd 663535 PDF 88/1/08/1/08 11:09:58:09:58 PPMM These reading tools will help you learn the material in this chapter.
    [Show full text]
  • Exploring Deep Oceanic Crust Off Hawai'i
    Workshop Reports Sci. Dril., 29, 69–82, 2021 https://doi.org/10.5194/sd-29-69-2021 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. Workshop report: Exploring deep oceanic crust off Hawai‘i Susumu Umino1, Gregory F. Moore2, Brian Boston3, Rosalind Coggon4, Laura Crispini5, Steven D’Hondt6, Michael O. Garcia2, Takeshi Hanyu7, Frieder Klein8, Nobukazu Seama9, Damon A. H. Teagle4, Masako Tominaga10, Mikiya Yamashita7,11, Michelle Harris12, Benoit Ildefonse13, Ikuo Katayama14, Yuki Kusano15, Yohey Suzuki16, Elizabeth Trembath-Reichert17, Yasuhiro Yamada18, Natsue Abe18, Nan Xiao18, and Fumio Inagaki18 1School of Geosciences and Civil Engineering, College of Science and Engineering, Kanazawa University, Kanazawa 920-1192, Japan 2Department of Earth Sciences, University of Hawai‘i at Manoa,¯ Honolulu, HI 96822, USA 3Lamont-Doherty Earth Observatory, Columbia University, Palisades, NY 10964, USA 4School of Ocean and Earth Science, National Oceanography Centre Southampton, University of Southampton, Southampton SO14 3ZH, UK 5Department of Earth, Environment and Life Sciences, University of Genoa, 16126 Genoa, Italy 6Graduate School of Oceanography, University of Rhode Island, Narragansett, RI 02882, USA 7Research Institute for Marine Geodynamics, Japan Agency for Marine-Earth Science and Technology (JAMSTEC), Yokosuka 237-0061, Japan 8Department of Marine Chemistry and Geochemistry, Woods Hole Oceanographic Institution, Woods Hole, MA 02543, USA 9Department of Planetology, Graduate School of Science,
    [Show full text]
  • *Oceanology, Phycal Sciences, Resource Materials, *Secondary School Science Tdpntifitrs ESFA Title III
    DOCUMENT RESUME ED 043 501 SE 009 343 TTTLE High School Oceanography. INSTITUTION Falmouth Public Schools, Mass. SPONS AGPNCY Bureau of Elementary and Secondary Education (DHFW/OF) ,Washington, D.C. PUB DATE Jul 70 NOTE 240p. EDRS PRICt FDRS Price MP -81.00 HC-$12.10 DESCRIPTORS *Course Content, *Curriculum, Geology, *Instructional Materials, Marine Rioloov, *Oceanology, Phycal Sciences, Resource Materials, *Secondary School Science TDPNTIFItRS ESFA Title III ABSTRACT This book is a compilation of a series of papers designed to aid high school teachers in organizing a course in oceanography for high school students. It consists of twel7p papers, with references, covering each of the following: (1) Introduction to Oceanography.(2) Geology of the Ocean, (3) The Continental Shelves, (ft) Physical Properties of Sea Water,(e) Waves and Tides, (f) Oceanic Circulation,(7) Air-Sea Interaction, (P) Sea Ice, (9) Chemical Oceanography, (10) Marine Biology,(11) The Origin and Development of Life in the Sea, and (12) Aquaculture, Its Status and Potential. The topics sugoeste0 are intended to give a balanced ,:overage to the sublect matter of oceanography and provide for a one semester course. It is suggested that the topics be presented with as much laboratory and field work as possible. This work was prepared under an PSt% Title III contract. (NB) Title III Public Law 89-10 ESEA Project 1 HIGH SCHOOL OCEANOGRAPHY I S 111119411 Of Mittm. 11K111011Witt 010 OfItutirCm ImStOCum111 PAS 11t1 t10100ocli WC lit IS MIMI 110mMt MS01 01 Wit It1)01 *Ms lit6 il. P) Of Vim 01 C1stiOtS SIM 10 1011HISSI11t t#ItiS111 OMR 011C CO Mita 10k1)01 tot MKT.
    [Show full text]