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First Reflection seismic experiment in Oklahoma in 1921.

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Presentation on theme: "First Reflection seismic experiment in Oklahoma in 1921."— Presentation transcript:

1 First Reflection seismic experiment in Oklahoma in 1921

2 Seismic Reflection is the most important tool we have to image subsurface structure. Provides detailed imaging of approximately horizontal layering in the earth Reflection seismology is echo or depth sounding Reflection Seismology

3 A ship is moving and fires air- guns about every 10 s. The pulses travel downward and are partially reflected back up from the reflectors Waves are then recorded by seismic receivers Reflection Seismology

4 The result is a seismic section Provides a picture of the subsurface structure The resulting structure can be interpreted as stratigraphy Seismic Section

5 Yet, there are reasons that the section is NOT true. Vertical scale is not depth, but time Actual time is two-way travel- time (down and back). Can be converted to depth, but must know velocity structure. Seismic Section

6 If layering is not horizontal, reflections will not come from directly below the source. Problem solved using a migration algorithm. Seismic Section

7 There may be multiple reflections in addition to the primary reflections This makes artifacts. Algorithms exits to minimize. Seismic Section

8 The time to travel to a receiver a distance x away from the source is Normal Moveout (NMO) x: src—rec offset (m) T 0 : vertical travel-time ∆t(x): moveout wrt offset h i : i th layer thickness (m) V: layer velocity S: source coordinate R: receiver coordinate A: reflection point (mid- point of ray for flat layers).

9 Normal Moveout Derivation h v S M R 0 x/2 x L L Normal moveout derivation t: travel-time L: right triangle hypotenuse v: velocity of layer (km/s) t 0 : two-way time x: source-receiver offset h: layer thickness (km)

10 Rearrange NMO equation for the velocity of the layer t o : two way travel-time (s) x: offset from src-rec (km) Δt(x): moveout at x-offset (s) Normal Moveout (NMO)

11 What velocity should be used for two layers? Answer: Root Mean Square (RMS) velocity τ i : one wave interval time (top to bottom time) Multiple Layers Can solve for v 2 Can iterate this procedure for deeper layers

12 Another way to calculate velocity of any layer B index: layer bottom T index: layer top v layer : layer velocity t B : 2-way tt to layer bottom t T : 2-way tt to layer top v rms,B RMS velocity to bottom v rms,T RMS velocity to top Multiple Layers: Dix formula

13 Almost always the reflections are weak and are hard to recognize because of inevitable noise To increase the signal-to-noise ratio, stacking is used Take repeated measurements and average Signal (reflections) add constructively and noise cancels Stacking

14 Finding layer velocities and stacking done simultaneously Try range of v rms NMO correct the times of the seismograms If the v rms is correct strong reflections are found If v rms is incorrect Reflections are not found. Stacking

15 Dipping Reflectors If a reflector is dipping, its apparent position and dip are wrong in an unmigrated section. Wave raypaths are least-time paths and hence reflect from up dip points. Unmigrated reflector is shallower and with less dip. Travel-time hyperbola offset: h (thickness), alpha (dip)

16 Curved Reflectors: Syncline If a interface is sufficiently curved, there can be more than one reflection returned from the interface: multi-pathing. As the shot point is shifted from 1 to 10, three arrivals are produced that make a ‘bow tie’ travel-time pattern. Migration can ‘unwrap’ the bow- tie to improve the quality of the migrated image.

17 Curved Reflectors: Anticline Anticline has simpler response wrt Syncline. An anticline seismic image is broadened At edges of anticline two arrivals exist.

18 Migration Correcting for the position and shape of the reflector is called migration Complicated and requires large amounts of computer time Be aware of possible distortions in un-migrated sections

19 Faulted Reflectors Consider a point source (reflector). The distance that a source-receiver measures is on the arcs shown Multiple source-receivers produce the reflection hyperbola shown A stepped reflector behaves normally except near the step Produces a reflection hyperbola Difficult to tell position of fault Migration removes diffraction effects and reveals features more clearly

20 Faulted Reflectors Migration removes diffraction effects and reveals features more clearly

21 Multiple Reflections The positions of multiples can be anticipated from the position of the primary reflectors However, sometimes it is difficult to recognize a primary reflector that comes in with the same TWT as the multiples Can be distinguished Moveout for the primary is less than for the multiple, so it stacks using a higher velocity

22 Most common source is an Air Gun –Produces P-waves (no S-waves) Receiver is a hydrophone –Microphone that responds to change in pressure –Mounted at regular intervals and towed behind the ship in a streamer Marine Surveys

23 Most common source is an explosion –Buried small charge fired by detonator Receiver is a geophone –Often times in clusters to improve s/n ratio Moving the system on land is much harder resulting in much more expense Land Surveys

24 The output of each receiver is connected to an amplifier Data is recorded digitally –sampled at regular intervals, often only 1 msec Data Recording

25 Common Depth Point Stacking Common Depth Point Stacking (CDP) uses rays that have all reflected from the same part of the interface Uses pairs of shot points and receivers that are symmetrical about the reflector point CDP stacking gives better data for computing velocities and stacking Number of channels that are added are the fold 240-fold stacking is common

26 Static Corrections In Land Surveys, significant topography has to be corrected for Additionally, must take into account the effect of the topsoil and other weathered layers Called Static Corrections puts data on convenient horizontal plane

27 Data Display Deep reflections are weaker due to energy loss and spreading Sometimes amplified to compensate- equalization

28 Vibroseis Vibroseis produces a continuous wave with changing frequency To find the travel time, the recorded signal is shifted in time until the entire waveform matches the source The energy required is small An advantage where non-intrusive is preferred

29 Vibroseis The waves are generated by a vehicle with a plate that presses rhythmically against the ground instantaneous force of 15 tonnes 1 metric tonne =1000 kg or 2205 lb Frequency is swept from 10 to 100 Hz over 30 sec Sometimes several vehicles operate in unison increases energy has reached Moho (30 km)

30 What is a Reflector? Rays are reflected when they meet an interface Abrupt change in seismic velocity How abrupt? We can define the acoustic impedance

31 Reflection Coefficient Reflection coefficient Transmission coefficient Only valid for normal rays

32 Reflection Coefficient Because the S-wave velocity and the P-wave velocities are different, their coefficients of reflection can also differ. Sometimes S-waves are reflected more strongly than P- waves. Consider the ratio of reflected energy Check on this

33 Reflection Coefficient Example Calculate the reflection coefficient of sandstone overlying limestone. Suppose that the properties of sandstone are at the bottom of their ranges while those of limestone are at the top

34 Reflection Coefficient Example Suppose instead we have materials with different properties: Lithological boundary, but no seismic boundary In reality, may produce a weak reflector

35 Bright Spot The interface in a hydrocarbon reservoir between a gas layer and underlying oil or water produces a strong reflection Called a ‘bright spot’ A strong, horizontal ‘bright spot’ Evidence for presence of gas

36 Vertical Resolution Suppose two interfaces could be brought progressively closer together Reflected pulses would overlap more and more At some point, the pulses cannot be resolved The shape of the combined pulses also changes

37 Vertical Resolution Often the two interfaces are two sides of a thin layer sandwiched within another Shale layer within Sandstone One interface has positive R and other negative Negative R means that the reflected pulse is inverted Interference Can produce no reflected wave

38 Vertical Resolution Since the pulse reflected from the lower interface has to travel further by twice the separation of the interfaces Difficult to resolve when they are less than half a wavelength apart Vertical resolution can be improved by using a shorter pulse Shorter pulses are more rapidly attenuated Must compromise between resolution and depth penetration

39 Vertical Resolution Another situation where there is no reflection is when an interface is a gradual change of velocities and densities extending over more than about half a wavelength, rather than being abrupt Can be thought of as many thin, sandwiched layers Interference causes cancelation Lithological boundary with no seismic reflector

40 Synthetic Reflection Seismograms Can be used to improve interpretation First, choose a pulse that corresponds to the source Next, calculate the reflection and transmission coefficients Based on borehole data Propagate the pulse ‘down through the layers’

41 Synthetic Reflection Seismograms If there are several interfaces closer together than the length of the average wavelength of the pulse, the reflected pulses often combine to give peaks that do no coincide with any of the interfaces

42 3D Surveying We are often interested in the form of structures perpendicular to the seismic sections we have been studying There can be reflections from dipping interfaces outside the plane of the section Sideswipe This can be addressed by using a regular grid on the surface (3D survey) Often times the grid is on 50 m spacing

43 3D Surveying A CDP gather comprises pairs of shot points and receivers from all around the CDP Stacking, migration follow the same principles Obviously more difficult and computer intensive

44 3D Surveying We can think of the reflectors revealed as being embedded in a block Can take ‘slices’ in any direction More sophisticated processing can reveal properties of the rock such as porosity Determines the amount of hydrocarbon that a rock can hold

45 3D Surveying May want to add the image from plate 6 of the book here and comment on the use of porosity

46 Time-Lapse Modeling By repeating surveys at intervals, the extraction of hydrocarbons can be followed and remaining pockets of oil detected Though 3D surveying is much more expensive, both for data acquisition and reduction, it can pay for itself in the increased understanding of the structure of hydrocarbon reservoirs

47 Forming Hydrocarbon Reservoirs Organic material (minute plants & animals) is buried in a source rock that protects it from oxidation (often clays in a sedimentary basin) Bacterial action operating at temperatures of 100 to 200°C changes the organic matter into droplets of oil The droplets are squeezed out of the source rock Being lighter than water, usually move upward Deformation can cause them to move sideways Impervious cap rock (shale) prevents leakage To be extractable, reservoir rock must be porous and permeable To be commercially viable, must be concentrated

48 Hydrocarbon Traps Structural Traps result from tectonic processes Folds, domes, faults, etc

49 Hydrocarbon Traps Stratigraphic Traps are formed by lithological variation in the strata at the time of deposition Lens of permeable and porous sandstone or a carbonate reef, surrounded by impermeable rocks

50 Hydrocarbon Traps Combination Traps have both structural and stratigraphic features Where low density salt is squeezed upwards to form a salt dome, both tilting strata and causing hydrocarbons to concentrate as well as blocking off their escape

51 Hydrocarbon Traps How can hydrocarbon traps be located with seismic reflection? Easiest to recognize are structural ones. Stratigraphic traps which have tilted reservoir rcoks terminating upwards in an unconformity are also fairly easy to spot Bright spots show presence of gas-oil or gas-water interface Smaller and harder to recognize traps are being exploited High quality surveys necessary Closely spaced stations, high resolution sources Precise processing of data

52 Sequence Stratigraphy Sequence stratigraphy is the building up of a stratigraphy using seismic sections Can provide constraints on global sea-level change Used as a dating tool Possible because chronostratigraphic boundaries (surfaces formed within a negligible interval of time) are also often reflectors Stratigraphic sequence Sequence of strata of common genesis bounded by unconformities

53 Sequence Stratigraphy How a sequence is built up and terminated depends on the interplay of deposition and changes in sea level (eustatic changes) Complex, but all we are concerned with is the relative sea level changes while the sediments are being deposited

54 Sequence Stratigraphy Consider deposition along a coastline where sediments are being supplied by a river, and sea level is constant Prograding succession Thinning at top Top lap

55 Sequence Stratigraphy Consider deposition along a coastline where sediments are being supplied by a river, and sea level is rising steadily Successive near horizontal layers Onlap where they butt up to the coastline

56 Sequence Stratigraphy Slow rise in sea level (and constant sea level) results in progradation (lateral buildup of stratigraphy) Rapid rise of sea level results in aggradation (vertical buildup of stratigraphy

57 Sequence Stratigraphy An unconformity defines the boundary of a sequence occurs when sea level falls fast enough for erosion rather than deposition to occur Moderate sea level retreat Truncates tops of beds Rapid sea level retreat Erosion cuts laterally

58 Sequence Stratigraphy Beds that end are termed discordant Appear in seismic sections as reflectors that cease laterally Can be used for working out the history of deposition and erosion

59 Sequence Stratigraphy and Eustasy Sequence stratigraphy provides a record of the changes in local relative sea level Types and volumes of various facies within the sequence provides constraints on the amounts of rise and fall of sea level Fossils taken from boreholes can be used to estimate their times Correlations between widely separated basins can be used to determine global sea level changes.


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