Presentation is loading. Please wait.

Presentation is loading. Please wait.

Nils Holzrichter, Jörg Ebbing

Published byTimothy Stewart Modified over 6 years ago

Similar presentations

Presentation on theme: "Nils Holzrichter, Jörg Ebbing"— Presentation transcript:

1 Nils Holzrichter, Jörg Ebbing
Modelling the lithospheric structure of the Arabian Peninsula with satellite gravity gradients Nils Holzrichter, Jörg Ebbing Department of Geosciences, Kiel University

2 GOCE for global and regional Moho
Global Moho from GOCE (GEMMA project, Reguzzoni et al. 2013) Moho depth (Hansen et al. 2007) Crust Moho => Lith. Mantle Base lithosphere =>

3 GOCE for global and regional Moho
Moho depth (Hansen et al. 2007) Global Moho from GOCE (GEMMA project, Reguzzoni et al. 2013) Crust Moho => Lith. Mantle Base lithosphere =>

4 Motivation „Local“ modelling of the crustal and upper mantle
structures accounting for all gravity gradients What is the density distribution and structure of the lithosphere? Does the use of full gravity gradients improve the modelling procedure?

5 Motivation Steps in this project:
Took an old model fitted for Gzz as a starting point. Used gravity gradients in an orbit height of 225 km. Checked the local fit of Crust 1.0. Forward modelled the area to fit all gravity gradient components.

6 Constraints and forerunner projects

7 Additional (old) information
Hansen et al. 2007 Bouguer anomaly (EGM2008) Top Basement (Konert et al. 2001) Topography

8 Seismological modelling result
Hansen et al. 2007 Hansen et al. 2007

9 Moho depth by satellite gravity gradient inversion (Ebbing et al
Gzz=Full Z0=30 km Dr= 350 kg/m3

10 Moho depth by satellite gravity gradient inversion (Ebbing et al
Gzz=Full Z0=30 km Dr= 350 kg/m3

11 Modelling improvement with GOCE gravity gradients

12 Input fields Topographic corrected gravity gradients in an orbit height of 225 km.

13 Comparison to Crust 1.0 Crustal model (Crust 1.0) added to a simple LAB model to calculate modelled gradients. Laske et al.

14 Crust 1.0 Measured fields Calculated fields

15 From crustal thickness to full lithospheric model
Extension of the existing model to a full lithospheric model Correlation with seismic constraints Adjustment to all gravity gradients Modelling of data in 225 km orbit height

16 The initial model had constant density layers: Base of the lithosphere
Gxx Gxz Gzz calculated measured Measured fields The initial model had constant density layers: Base of the lithosphere Isotherms: 1100, 900 and 700 degrees Celsius Moho Base middle crust and base upper crust Top basement 2700 2900 2700 2700 2930 2900 3000 3340 3300 3335 3280 3320 3285 3290 3310 3300

17 Measured fields Calculated fields Gxx Gxz Gzz calculated measured 2700
2900 2700 2700 2930 2900 3000 3340 3300 3335 3280 3320 3285 3290 3310 3300 Calculated fields

18 1 density gradient in crust
Modification 1 density gradient in crust 2700 3000 2900 3300 2930 3280 3285 3290 3275 Gxx Gxz Gzz calculated measured 3340 3335 3320 3310 Measured fields Calculated fields

19 3 New deep lithosphere and updated Moho
Modification 2 Lower Crust 3 New deep lithosphere and updated Moho Gxx Gxz Gzz calculated measured Measured fields 2700 2700 2900 2900 3000 2900 3300 3280 3285 3290 3275 Calculated fields

20 4 lateral crustal variation (Arabian Sea)
Modification 4 lateral crustal variation (Arabian Sea) 2700 3000 2900 3300 2930 3280 3285 3290 3275 Gxx Gxz Gzz calculated measured Measured fields Calculated fields

21 Final maps Measured fields Calculated fields

22 Final maps Measured fields Top Basement (Konert et al. 2001)

23 Use of new density models
The density models are used to improve heat flow modelling and maturity maps of the area.

24 Conclusions The full tensor gradient modelling add constraints to the density modelling which improve the result. The modelling shows lateral and vertical density variations in the crust. The non-diagonal components provide information about lateral density variations and the strike of the anomalous bodies

25 Comparison to Crust 1.0 and GEMMA
Model 1: Moho (GEMMA/Crust) Model 2: Density variations (Crust 1.0) added to a simple LAB model to calculate modelled gradients. Moho of Crust 1.0 model Moho of GEMMA model Laske et al. M. Reguzzoni et al.

26 GEMMA Moho Model fits the shape of some anomalies, but in general this model provides a poor fit, especially the amplitudes are too large.

27 I2^(1/3) from measured signal I2^(1/3) from calculated signal

Download ppt "Nils Holzrichter, Jörg Ebbing"

Similar presentations

Satellite gravity gradients for lithospheric structure R. Hackney, H.-J. Götze, S. Schmidt Institut für Geowissenschaften, Abteilung Geophysik Christian-Albrechts-Universität.

Satellite gravity gradients for lithospheric structure R. Hackney, H.-J. Götze, S. Schmidt Institut für Geowissenschaften, Abteilung Geophysik Christian-Albrechts-Universität.
SPP 1257 Modelling of the Dynamic Earth from an Integrative Analysis of Potential Fields, Seismic Tomography and other Geophysical Data M. Kaban, A. Baranov.

SPP 1257 Modelling of the Dynamic Earth from an Integrative Analysis of Potential Fields, Seismic Tomography and other Geophysical Data M. Kaban, A. Baranov.
An estimate of post-seismic gravity change caused by the 1960 Chile earthquake and comparison with GRACE gravity fields Y. Tanaka 1, 2, V. Klemann 2, K.

An estimate of post-seismic gravity change caused by the 1960 Chile earthquake and comparison with GRACE gravity fields Y. Tanaka 1, 2, V. Klemann 2, K.
Problem 1 The corrections can be larger than the anomaly Stat.Time T Dist. (m) Elev. (m) Reading (dial units) Base reading at time T Drift corr’d anom.

Problem 1 The corrections can be larger than the anomaly Stat.Time T Dist. (m) Elev. (m) Reading (dial units) Base reading at time T Drift corr’d anom.
The general equation for gravity anomaly is: where:  is the gravitational constant  is the density contrast r is the distance to the observation point.

The general equation for gravity anomaly is: where:  is the gravitational constant  is the density contrast r is the distance to the observation point.
The Earth’s Structure Seismology and the Earth’s Deep Interior The Earth’s Structure from Travel Times Spherically symmetric structure: PREM - Crustal.

The Earth’s Structure Seismology and the Earth’s Deep Interior The Earth’s Structure from Travel Times Spherically symmetric structure: PREM - Crustal.
Chapter 17 Earth’s interior. Earth’s interior structure Earth is composed of three shells; –Crust –Mantle –Core.

Chapter 17 Earth’s interior. Earth’s interior structure Earth is composed of three shells; –Crust –Mantle –Core.
Large Scale Gravity and Isostasy

Large Scale Gravity and Isostasy
Scientists divide the Earth

Scientists divide the Earth
Dynamic topography, phase boundary topography and latent-heat release Bernhard Steinberger Center for Geodynamics, NGU, Trondheim, Norway.

Dynamic topography, phase boundary topography and latent-heat release Bernhard Steinberger Center for Geodynamics, NGU, Trondheim, Norway.
PIVETTA T., BRAITENBERG C. Dipartimento di Geoscienze, Università di Trieste, Italy, THE LITHOSPHERE STRUCTURE BENEATH.

PIVETTA T., BRAITENBERG C. Dipartimento di Geoscienze, Università di Trieste, Italy, THE LITHOSPHERE STRUCTURE BENEATH.
Geology of the Lithosphere 2. Evidence for the Structure of the Crust & Upper Mantle What is the lithosphere and what is the structure of the lithosphere?

Geology of the Lithosphere 2. Evidence for the Structure of the Crust & Upper Mantle What is the lithosphere and what is the structure of the lithosphere?
LaCoste-Romberg.

LaCoste-Romberg.
Thermal structure of old continental lithosphere from the inversion of surface-wave dispersion with thermodynamic a-priori constraints N. Shapiro, M. Ritzwoller,

Thermal structure of old continental lithosphere from the inversion of surface-wave dispersion with thermodynamic a-priori constraints N. Shapiro, M. Ritzwoller,
The Four Candidate Earth Explorer Core Missions Consultative Workshop 12-14 October 1999, Granada, Spain, Revised 2006-01-05 by CCT GOCE S 43 Science and.

The Four Candidate Earth Explorer Core Missions Consultative Workshop October 1999, Granada, Spain, Revised by CCT GOCE S 43 Science and.
Upper mantle structure beneath the eastern Colorado Plateau and Rio Grande rift revealed by Bouguer gravity, seismic velocities and xenolith data Mousumi.

Upper mantle structure beneath the eastern Colorado Plateau and Rio Grande rift revealed by Bouguer gravity, seismic velocities and xenolith data Mousumi.
The Four Candidate Earth Explorer Core Missions consultative Workshop 12-14 October 1999, Granada, Spain, Revised 2006-01-05 by CCT GOCE S 23 The gravity.

The Four Candidate Earth Explorer Core Missions consultative Workshop October 1999, Granada, Spain, Revised by CCT GOCE S 23 The gravity.
Gravity: Gravity anomalies. Earth gravitational field. Isostasy. Moment density dipole. Practical issues.

Gravity: Gravity anomalies. Earth gravitational field. Isostasy. Moment density dipole. Practical issues.
AN ORGANISATION FOR A NATIONAL EARTH SCIENCE INFRASTRUCTURE PROGRAM Capricorn Transect : Lithospheric Background B.L.N. Kennett Research School of Earth.

AN ORGANISATION FOR A NATIONAL EARTH SCIENCE INFRASTRUCTURE PROGRAM Capricorn Transect : Lithospheric Background B.L.N. Kennett Research School of Earth.
J. Ebbing & N. Holzrichter – University of Kiel Johannes Bouman – DGFI Munich Ronny Stolz – IPHT Jena SPP Dynamic EarthPotsdam, 03/04 July 2014 Swarm &

J. Ebbing & N. Holzrichter – University of Kiel Johannes Bouman – DGFI Munich Ronny Stolz – IPHT Jena SPP Dynamic EarthPotsdam, 03/04 July 2014 Swarm &

Similar presentations

Ads by Google