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Holocene Marine Deposits: modelling self-weight consolidation N. Keith Tovey 1 , Mike Paul 2 , Yap Chui-Wah 3 , and Simon Tovey 4. 1 School of Environmental Sciences, University of East Anglia, Norwich, NR4 7TJ, UK 2 School of Life Sciences, Heriot Watt University, Edinburgh,

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slide1

Holocene Marine Deposits: modelling self-weight consolidation

    • N. Keith Tovey1 , Mike Paul2,
    • Yap Chui-Wah3, and Simon Tovey 4

1School of Environmental Sciences, University of East Anglia,

Norwich, NR4 7TJ, UK

2 School of Life Sciences, Heriot Watt University, Edinburgh,

EH14 4AS, UK

3 Singapore Meteorological Service, Changi Airport, Singapore 918141

4 101 Media Ltd, Keswick Hall, NR4 6TJ, Norwich, UK

  • Acknowledgements:
  • Geotechnical Engineering Office, Hong Kong
  • Civil Engineering Office, Hong Kong
  • Prof. Muneki Mitamura, Osaka
  • Carolyn Sharp, University of East Anglia
slide2

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide3

The Problem

  • What effect does self-weight consolidation (auto-compaction) have on our understanding of Marine Sequences?
  • What processes are involved?
  • What are the magnitudes of such effects?
  • How easy is it to correct for these effects?
slide4

Why are such studies of relevance?

Interpretation of sequences is often done on a linear length basis.

i.e. two points in a sequence may be dated and a sedimentation rate estimated from dates anddistancesbetween the two points.

This does not allow for self-weight consolidation - strictly it should be done using a linear mass interpolation - rarely is this the case.

This is of particular importance in unravelling Holocene sequences where theapparentdeposition rate is of the order of 0.5 - 5 mm per year.

It is of significance in dating studies and also estimation of palaeo-water depths in tidal modelling etc.

slide5

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide6

Isopach of M1 Unit at Chek Lap Kok

Good quality continuous cores are available from Hong Kong to depths of 20+m

slide8

Simplified Sequence of Deposition

During last inter-glacial

deposition of unit M2

When sea level fell, surface layer was exposed to desiccation, oxidation, pedogenesis, etc.

~10m

M1

In the Holocene, the sea probably covered the area around 6000 - 8000 years ago

deposition of unit M1

T1

M2

slide9

From core record, several different sequences have been identified

Classification after Yim

Present work models Holocene sequence

slide10

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide11

Clay

Sand

Consolidation in Marine Sediments

Two pore pressures to consider

  • Hydrostatic pressure changes from sea level changes are insignificant with regard to sediment compression.
  • Excess pore pressures are of critical importance.

Assumes sand body is continuous and “daylights” to sea bed -i.e. two-way drainage.

Single drainage - implies sand body is discontinuous and does not “daylight”

slide12

Decompaction of Deposits

  • During deposition, successive layers will cause under-lying layers to compress
  • Dividing the total thickness by the time interval will lead to an under-estimation of true deposition rates.
slide13

Decompaction of Deposits

  • If the Void Ratio is known, then the saturated bulk unit weight (i) in the ith layer is given by:-
    • where Gs is Specific gravity
  • The stress i at the mid point of the ith layer is given by:-

However, ei depends on v(i)

slide14

Decompaction of Deposits

  • First assume a value of ei (say 1.0) and evaluate i in the ith layer from:-
  • Now determine i at the mid point of
  • the ith layer:-
  • If the e -v relationship is known
  • determine a revised value of ei and
  • repeat above two steps iteratively.

Must work down through layers not upwards!

slide16

e1 = 3.1269 - 0.841 log()

R2 = 0.9954

The parameter e1 = 3.1269 [void ratio at 1 kPa] and gradient of line Cc are used in the algorithms.

slide17

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide18

This is an interesting result:

The relationship holds over all three units!

It means that we only need to determine Cc

slide19

However, an even more interesting correlation emerges

e1 = 0.8154 + 2.8473 Cc

It appears that data from Hong Kong and Scotland follow same trend

slide21

Omega Point

If this relationship were to hold more generally, then we can predict e1 from Cc

slide22

M2

M1

Gassy sediments

T1

Inclusion of many more data points still confirms a relationship

e1 = 0.8662 + 2.7111 Cc

R2 = 0.9775

slide23

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide24

For typical Holocene deposits, the true sedimentation rate may be up to 2+ times the raw sedimentation rate.

slide25

What is a typical value for sedimentation rate?

  • Assume 10 m Holocene sequence and Cc approximately 1.0.
  • If sea level rose about 6500 years ago, then raw sedimentation rate is about 1.5 mm per year
  • But after correction, the true rate for the Hong Kong M1 unit is > 3 mm per year.
  • Any modelling must use layers no thicker than this.
slide26

A Problem

  • Measurement of Cc requires special testing

But estimates are available using Liquid Limit measurements

slide27

An alternative if neither consolidation or liquid limit data are not available

-valid for Holocene - i.e. degree of saturation is 100% .

Assume a detailed moisture/water content can be measured at moderate/high resolution.

  • Now determine i at the mid point of the ith layer:-
  • e -v can be plotted directly and hence Cc can be deduced.
slide28

Porosity varies significantly in uppermost 2m.

Void ratio of 2 is equivalent to a porosity of 0.667

Void ratio of 4 is equivalent to a porosity of 0.8

slide29

The values of moisture content are almost always above the mean prediction suggesting a more open structure than expected

slide30

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide31

Equilibrium self-weight consolidation analysis assumes that after each increment all excess pore pressure is dissipated.

  • Conventional wisdom suggests that with all normal sedimentation rates, dissipation will be complete within an annual deposition cycle.
  • This is true provided drainage paths are NOT long.
  • However, will this be true for deep sequences where drainage paths are long?
slide32

The governing equation for dissipation of pore pressure (u) by:-

where cv is the coefficient of consolidation and may be found from:

where k is permeability and mv is determined from Cc

To proceed we need a relationship to determine k

slide33

There appears to be a relationship between void ratio and permeability

However, this relationship is likely to vary from one location to another.

slide34

The dynamic model

  • Properties of each layer vary as a result of self-weight consolidation.
  • For a given value of Cc determine
    • equilibrium void ratio and hence unit weight and stress for each layer
    • permeability from e - k relationship
  • and hence estimate
    • mv
    • cv.

If data exists, Cc can also be allowed to vary between layers

slide35

Choice of initial layer thickness

The void ratio varying rapidly in top 1 - 2m, and layer thickness must reflect this and also be able to model and annual accumulation.

> Layer thicknesses ~ 3mm should be used.

> ~ 3000 layers

  • A Problem:
    • simple analysis using FTCS method will require time steps < 100 secs for stability - very computer intensive.
    • Crank Nicholson method is stable irrespective of time step, although 100 iterations per year are still needed for spatial precision.
slide36

Crank-Nicholson requires inversion of matrices which have the number of rows and columns equal to number of layers.

  • Solution - use layer thickness which progressively double at greater depths.
  • Current model starts with 150 layers
  • But, number of layers increases each year, and time to model 500 years becomes very long ~ 10 - 20 hours with modern computers.
  • However trends can be seen
slide37

Results of pore pressure dissipation over first 10 years

- annual increment as determined by equilibrium analysis

Below 3m there is no dissipation in year 1. There is evidence of a small amount of dissipation after 10 years.

slide38

Results from 10 - 500 years - assume Holocene depth - 10m

Partial dissipation is taking place at base of Holocene - dissipation lines are getting closer together

slide39

The presence of excess pore pressures would lead to higher water contents than predicted by steady state analysis

Could this be difference be a result of bio-turbation?

Unlikely to be the sole cause as deviation increases with depth just as residual pore pressures do.

slide40

Recent results from Japan

  • 18 consolidation tests were done on a single borehole
  • different values of Cc were measured.
  • modify steady state analysis to allow for this variation
  • predicted and actual water are similar at base of Holocene
  • implies full dissipation of pore pressure > double drainage.
slide41

Holocene Marine Deposits: modelling self-weight consolidation

1. Background to self-weight consolidation issues

2. Site Locations

3. Equilibrium Self-Weight Compaction

4. Existence of Omega Point?

5. True Sedimentation Rates

6. Modelling pore-pressure dissipation

7. Conclusions

slide42

Conclusions

  • raw sedimentation rates significantly underestimate true sedimentation rates by a factor of 2 or more
  • from consolidation theory, estimates of true porosity and hence sedimentation rates are possible
  • excess pore pressures arising from annual deposition remain at the end of the year in sequences thicker than about 2m
  • pore pressures continue to build up each year
    • > higher than predicted equilibrium moisture contents
  • the excess moisture content distribution gives an indication of drainage conditions prevailing.
slide43

The future

  • correlation of excess pore water pressures with excess water content - does this explain the full difference between steady state model and actual data points?
    • > need to model over the whole Holocene period
  • develop model to include pre-Holocene layers
    • > estimates of palaeo-hydrology

And finally:

The research in this paper is a direct consequence of discussions held at the 2nd Annual Meeting of IGCP-396 in Durham UK (1997).

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