8. ocean crustal structure and seismic reflection william wilcock
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OCEAN/ESS 410. 8. Ocean Crustal Structure and Seismic Reflection William Wilcock. Lecture/Lab Learning Goals. Know the basic structure of the oceanic crust as determined from ophiolite studies Understand how oceanic crustal structure is linked to mantle melting and volcanic processes - PowerPoint PPT PresentationTRANSCRIPT
8. Ocean Crustal Structureand Seismic Reflection
William Wilcock
OCEAN/ESS 410
Lecture/Lab Learning Goals
• Know the basic structure of the oceanic crust as determined from ophiolite studies
• Understand how oceanic crustal structure is linked to mantle melting and volcanic processes
• Understand what seismic impedance is and how it controls the amplitude of seismic
• Know how seismic reflection data is collected• Know how reflection data is stacked and converted into a
seismic record section• What can seismic record sections tell you? - LAB
Melting beneath mid-ocean ridges
The melt rises out of the mantle because it is buoyant (less dense than the mantle)
Ophiolites
What will happen when the Juan de Fuca Ridge collides with the North American Plate?
30
Ophiolites around the world
Ophiolites - Remnants of oceanic crust
•The spreading center collides with a subduction zone.
•As the two plates converge the spreading center is thrust on top of the downgoing plate to form the ophiolite.
Oman
Ophiolite Sequence
Mantle
Crust-Mantle Interface (“Moho”)
Gabbro layer
0
6
3
Dep
th, k
m
Gabbros (layered) - they can also be un-layered (massive)
Sheeted dike layer
- “feeder channels” for basaltic lava rising from below
- The cracks extend over large distances beneath ridges
Sheeted dike layer
Sheeted dike layer
Pillow basalt layer
Pillow lavas
Pillow basalt layer
- Lavas extruded onto ocean floor at a spreading center
Sediment layer
Pelagic sediments deposited above oceanic crust basalts
Seismic Reflection
Reflections from Interfaces
When a downgoing P-wave meets an interface, a portion of the wave is reflected.
Acoustic (Characteristic) impedance
- An inherent property of the medium- Depends on sound speed (or seismic velocity) and
density - Pressure generated by vibration of molecules of a
particular medium at a given frequency
Amplitudes of Reflections for vertical rays
A0
V1, 1
V2, 2
The amplitude of the reflected and transmitted phase depends on the seismic velocity, V and the density, in each layer.
Larger contrasts in impedance result in large amplitude reflections
Marine Reflection Seismology - Airgun Sources
Reflection data is relatively easy to acquire in the oceans. Seismic sounds (shots) can be generated with arrays compressed air guns (airguns) towed behind the ship
Marine Reflection Seismology - Hydrophone Streamers
The airgun shots are recorded by arrays of hydrophones towed behind the ship in a streamer. The seismic streamers contain 1000’s of hydrophones and can be >10 km long. A modern 3-D seismic ship will tow several (the records is 20) streamers.
Marine Reflection Seismology - Geometry
The streamer records waves reflected from interfaces
Marine Reflection Seismology - Geometry
The streamer records waves reflected from interfaces
Marine Reflection Seismology - DataThe seismic data recorded for a particular shot will look display a geometric effect termed “normal moveout” (NMO) which reflects the increased distance the wave travels for as the source-receiver offset increases
Offset
Tim
e, sTime
X0
Marine Reflection Seismology - Sorting RecordsThe records are sorted so that they all have the same mid-point (Common Mid-Point - CMP)
Marine Reflection Seismology - Airgun SourcesThe seismic records can be corrected for geometric affects and stacked (summed) to produce a single record for the reflections below each each point
Before Geometric Correction
After Geometric Correction
Stacked (summed)
Marine Reflection Seismology - Filled Wiggle PlotsStacked records are plotted on the same plot with the horizontal axis showing position along the profile. Rather than showing lines for each record the plots often show filled regions for positive (or negative) displacements
Tim
e, s
Position
A reflection profile across the East Pacific Rise
Reflections come from the seafloor, the base of layer 2A (pillow basalts), the axial magma chamber (AMC) and the Moho (M)
Intersecting Record Sections from the East Pacific Rise
0
6
3
Dep
th, k
mStructure of a mid-ocean ridge crust
molten
2A
Moho
Layered Gabbro
Peridotite (Mantle)
Endeavour segment of
Juan de Fuca Ridge
TW
TT
(s)
AMC
2A/2B