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The outer compositional shell above the mantle. Crustal thickness and density variations contribute to surface topography and gravity; crust and mechanically defined lithosphere are different boundaries.

Approximate gravitational compensation of loads by subsurface mass redistribution. Airy and Pratt models use local column balances; flexural support spreads the load laterally. Real surface topography can also be maintained by dynamic stresses.

The SE annotation identifies a secondary electron image. The specimen has an open network of ridges, thin walls and irregular cavities, with lateral features on the scale of tens to hundreds of nanometres when compared with the 500 nm bar. Exposed edges can emit secondary electrons from more than one nearby surface; inclined faces also have a larger near-surface escape fraction than a face perpendicular to the beam. These mechanisms make protruding rims conspicuous. Recesses can be dark because emitted secondary electrons are intercepted or collected less efficiently. A through-lens detector changes the collection geometry, so a simple one-sided illumination analogy is incomplete.^[ref]

An irregular porous relief with bright rims and darker recesses is consistent with the image. The cross-section below is an original illustrative geometry, rather than a reconstruction of a particular image line. A single secondary electron intensity map does not supply calibrated heights, prove that every dark patch is a through-hole, or distinguish charging from all material contrast. Repeat with specimen tilt, altered detector collection or reduced accelerating voltage, and compare backscattered electron or elemental signals before assigning a compositional cause.

A steady-current image is not supported by the electrical connection drawn. tunnelling atomic force microscopy requires a conducting AFM probe, an applied bias voltage and a continuous return path from the contacted region to the current amplifier. graphene is conducting, but a flake on insulating glass is not electrically grounded merely because the other side or edge of the glass is earthed. Charging transients or displacement current are not its steady conductivity. Add a metal contact actually touching the graphene before using its current contrast; ordinary force-based surface topography can still be recorded without that contact. The manufacturer's nanostructure measurements explicitly distinguish objects connected to conducting pads from unconnected particles on the same insulating substrate.^[ref]

quantitative nanomechanical mapping can image the flake without an electrical return path. Repeated AFM force curves provide surface topography, adhesion and deformation or effective elastic modulus channels. The step and differences in tip–surface interaction can distinguish graphene from glass. For an atomically thin supported sheet the contact response is strongly substrate dependent, so fitting a three-dimensional half-space contact model does not directly measure the intrinsic in-plane Young's modulus of free graphene. Calibrate the cantilever spring constant, deflection sensitivity and tip radius, use small loads, and compare bare substrate. The manufacturer's description specifies the force-curve origin of the mechanical channels.^[ref]

Conventional semiconductor scanning capacitance microscopy is not a reliable dopant-contrast image of this specimen as drawn. Its usual $dC/dV$ signal relies on a tip–insulator–semiconductor capacitance whose depletion region changes under AC bias. An isolated conducting graphene sheet on thick insulating glass provides neither that conventional depletion geometry nor a controlled charge reservoir; simply earthing glass does not supply one. Capacitive or electrostatic contrast may be detectable with a suitably designed back electrode, a contacted flake and an appropriate capacitance-sensitive instrument, but that is an additional electrical device specification. Force-based surface topography remains possible independently of the specialized capacitance channel.

Three suitable approaches give complementary contrast. tapping-mode atomic force microscopy supplies surface topography and an oscillation-phase image. It reduces lateral drag and is often effective for soft block copolymer domains. Its phase contrast depends on elastic response, adhesion, dissipation and operating setpoint together: a bright phase domain is not automatically the stiffer polymer. Check contrast as amplitude and setpoint change and use a known reference.

quantitative nanomechanical mapping fits the repulsive portions of many AFM force curves and separately maps effective elastic modulus, adhesion and deformation. It directly addresses the stiffness difference and limits maximum force. Its quantitative result depends on tip radius, force calibration, contact model, loading rate and film thickness; domains narrower than the contact footprint are mixed and the substrate can dominate a thin film. Use small indentation, substrate controls and a suitable viscoelastic interpretation.

friction force microscopy can reveal domains with different frictional and adhesive response, using torsional deflection during contact scans. It is simple and sensitive to surface chemistry, but continuous shear may deform or displace soft domains, and slope/topography can contaminate the lateral signal. Acquire trace–retrace pairs at several low normal loads and check reproducibility. Use a mechanical-modulus map to test the stiffness assignment; phase or friction contrast alone does not uniquely identify stiffness or chemical composition.

gravity and surface topography. gravity responds to all density structure, while surface topography records both load and support. First specify the reference field and measurement height. latitude and planetary rotation affect normal gravity. At elevation $h$, the reference field decreases approximately by $2gh/R$; a free-air gravity anomaly restores this elevation effect but retains topographic mass. A Bouguer gravity anomaly additionally subtracts an approximate topographic slab contribution $2\pi G{\rho }_{c}h$. terrain correction replaces the unrealistic slab near valleys and ridges, and spherical geometry matters over large areas. A density choice is required for these reductions; a numerical crustal density is not provided here.

In Airy isostasy, surface topography of height $h$ and crustal density ${\rho }_c$ is compensated by a root of thickness $b$ replacing mantle of density ${\rho }_m>{\rho }_c$. Equal column masses give ${\rho }_{c}h=({\rho }_m-{\rho }_c)b$. The positive gravity of the relief is partly cancelled by the negative density contrast of the root. At long wavelengths a compensated mountain can therefore have a modest free-air anomaly and a negative Bouguer anomaly. Pratt isostasy instead varies column density at a roughly common compensation depth. Neither model says that surface topography itself exerts no gravity.

Potential-field depth filtering makes wavelength crucial. In a planar Fourier approximation, a density interface at depth $z$ is attenuated by $e^{-kz}$ at horizontal wavenumber $k$. For a small Airy-compensated height perturbation and a compensation interface at depth $D$, the gravity-topography admittance is approximatelyLong wavelengths allow strong cancellation between load and root. At short wavelengths the root's gravity is filtered out, so the observed near-surface mass can dominate even if the column is compensated. In a flexural isostasy model, an elastic lithosphere supports and spreads the load; for downward deflection $w$ and imposed load $q$, $D_f{\nabla }^{4}w+\Delta \rho gw=q$, with $D_f=E{T}_e^3/[12(1-{\nu }^2)]$. Thus $w_k=q_k/(D_f{k}^4+\Delta \rho g)$, and the effective elastic thickness controls the support scale.

Estimate admittance from cross-spectra of gravity and surface topography, and compare its wavelength dependence and coherence with local-compensation, elastic-flexure and subsurface-load models. A primary Atlantic study sampled ship-track free-air gravity and bathymetry and compared their Fourier-domain relationship with compensation models, illustrating this observational route rather than inferring a root from the sign of one gravity value.^[ref] Check navigation, instrument drift, terrain/density reductions, sediment and water loads, and independent seismic crustal constraints. Density-depth trade-offs and mantle dynamic support make the inverse problem nonunique; surface topography and gravity together constrain support, but do not uniquely map every density anomaly.

mantle viscosity. A second, independent route concerns deformation rates rather than static compensation. glacial isostatic adjustment follows loading and unloading of a deformable Earth: an ice sheet depresses the surface, and subsequent removal leaves time-dependent uplift, horizontal displacement, sea-level and gravity changes. Fit dated relative sea-level indicators and raised shorelines together with geodetic displacement rates and a reconstructed ice/water load history to a viscoelastic Earth model. Relative sea level includes solid-surface motion, changing geoid and redistribution of ocean water; treating it only as local vertical rock motion biases the inference.

For scale, a sinusoidal surface perturbation of wavenumber $k$ on a uniform incompressible viscous half-space relaxes under gravity with ${\tau }_k\sim 2\eta k/(\rho g)$. A Maxwell material separately has a stress-relaxation scale ${\tau }_M=\eta /\mu$. These are different experiments and generally different times: rebound modes also involve gravity, spherical geometry, a layered mantle and elastic lithosphere. Fit a family of relaxation modes or a full load-history convolution, rather than equating every observed rebound time to $\eta /\mu$.

Use independent ice-margin, exposure-age and sea-level constraints to reduce the trade-off between ice history and viscosity; compare horizontal as well as vertical GNSS motions, and separate present ice loss, groundwater changes and tectonic signals from the older loading response. A primary global analysis jointly tested ice-history and mantle-response predictions against space-geodetic observations, rather than treating a local uplift rate as a unique viscosity measurement.^[ref]

postseismic relaxation probes shallower or faster relaxation after a stress perturbation, but must be distinguished from afterslip and poroelastic deformation. Long-wavelength geoid and mantle-flow models provide complementary constraints when density structure is estimated independently from seismic structure and mineral physics; unknown density-to-velocity conversion and boundary tractions remain trade-offs. Laboratory creep experiments constrain constitutive laws as functions of temperature, stress and grain size, but require a large extrapolation to geological conditions. Combine spatially and temporally distinct observations; there is no single directly measured mantle viscosity independent of depth, rheology and loading assumptions.

A local compensation model in which columns of different density reach a common compensation depth. Higher surface topography is associated with a less dense column; density variation replaces the variable-root mechanism of an Airy model.

A correction for the difference between real surrounding relief and the assumed simple topographic slab. Its computation needs terrain geometry and an assumed density, and can matter in rough surface topography.