@NASAMoonBase
Addendum A — Coupled (P)–(T)–thirst start-up and the humidity maintenance layer
Author’s note. The original text assumed a geologist’s familiarity with dry rock, capillary uptake, and a slow pressure–temperature ramp as one obvious object. That knowledge is not average. The coupled start-up was in the design; it was not written. I apologize to readers for the confusion. This addendum states the model that should have been in the main paper.
A.1 Intent, stated in full
Start-up is a single coupled process after the ice glaze is applied:
habitat pressure (P) is ramped
interior temperature (T) is ramped
bone-dry lunar basalt takes up the first water (thirst)
vapor then moves by advection and diffusion
frost and mineral fill act only where local conditions allow
When that start-up has sated the dry-rock sink and dropped permeability in a wall annulus, habitat humidity — kept by deliberate growing conditions — is only a maintenance layer. It is not a second invention and not a substitute for establishment.
A.2 Variables
Radial coordinate (r) measured from the tunnel axis. Inner wall at \(r = r_w\).
SymbolMeaning(c(r,t))water-vapor concentration(T(r,t))temperature(P(r,t))pore pressure\(\phi(r,t)\)porosity\(k(\phi,S_w)\)permeability\(\mathbf{q}\)Darcy volume flux\(S_w\)condensed-water / ice saturation of pore space\(c_{\mathrm{sat}}(T)\)saturation vapor concentration
A.3 Heat (the moving frost line)
Basalt thermal diffusivity is large compared with matrix vapor diffusivity. The freeze isotherm therefore moves as the heading is heated:
\[ (\rho c_p)_{\mathrm{eff}} \frac{\partial T}{\partial t} = \frac{1}{r}\frac{\partial}{\partial r} \left( r\,\lambda_{\mathrm{eff}} \frac{\partial T}{\partial r} \right) + Q_{\mathrm{phase}} \]
Inner boundary during the ramp: \(T(r_w,t) = T_{\mathrm{ramp}}(t)\), rising toward the habitat set-point (\(+10\) to \(+20\,^\circ\mathrm{C}\)). Far-field rock is the local conductive mean at depth. Latent heat \(Q_{\mathrm{phase}}\) is small compared with conduction into the mass, but should be kept if ice volume is large.
The 0 °C / frost contour is \(T(r,t) = T_{\mathrm{frost}}\). It is not fixed in a static heat map.
A.4 Flow and vapor (Darcy + Fick + thirst)
Pore pressure is forced by the habitat ramp at the wall. In connected porosity:
\[ \mathbf{q} = -\frac{k(\phi,S_w)}{\mu}\,\nabla P \]
Vapor mass balance:
\[ \phi\frac{\partial c}{\partial t} + \frac{1}{r}\frac{\partial}{\partial r} \big( r\,q_r\,c \big) = \frac{1}{r}\frac{\partial}{\partial r} \left( r\,D_{\mathrm{eff}} \frac{\partial c}{\partial r} \right) + S_{\mathrm{ads}} + S_{\mathrm{frost}} \]\[ D_{\mathrm{eff}} = D_{\mathrm{bulk}}\,\frac{\phi}{\tau}\,f(S_w) \]
The first term after the time derivative is advection (the pressurization the main text left implicit). The second is diffusion (Fick, as in the main text).
Thirst is a finite sink while the rock is still dry. A simple Langmuir form is enough to state the idea:
\[ S_{\mathrm{ads}} = -\rho_s A_s \frac{\partial \theta}{\partial t}, \qquad \theta = \theta_{\max} \frac{K c}{1+K c} \]
\(\theta\) is adsorbed water per unit mineral surface. \(S_{\mathrm{ads}}\) is large only until surfaces and the tightest throats are sated. After that, thirst is no longer the dominant term. This sink retards the humidity front. It loads the near wall first. It does not throw water metres outward faster.
Frost / condensate only where vapor exceeds local saturation:
\[ S_{\mathrm{frost}} = -k_{\mathrm{d}} \max\big(c-c_{\mathrm{sat}}(T),0\big) \]
Ice or film saturation then reduces porosity and permeability:
\[ \frac{\partial S_w}{\partial t} = -\frac{S_{\mathrm{frost}}}{\phi\,\rho_{\mathrm{ice}}}, \qquad \phi = \phi_0(1-S_w) \quad\text{(simple end-member)} \]\[ k = k_0 \left(\frac{\phi}{\phi_0}\right)^{n} g(S_w) \]
Mineral precipitation (carbonates, clays, sulfides) is an additional, slower sink of the same sign as \(S_{\mathrm{frost}}\), limited by water films and available dissolved carbon. It is not assigned CarbFix field rates unless those reactants and a liquid phase are actually present.
A.5 Boundaries and the glaze
At \(t=0\) the inner face carries a thin ice glaze: a finite surface reservoir, not the full pore-filling inventory.
During the early ramp, if \(T(r_w)\le 0\,^\circ\mathrm{C}\), that glaze can persist and feed vapor into \(\mathbf{q}\) and \(D_{\mathrm{eff}}\) under rising \(P(r_w,t)\).
When \(T(r_w)\) exceeds freezing, the glaze is no longer a frozen skin holding pressure behind ice. The inner boundary becomes humid, pressurized air at the habitat ramp values:
\[ P(r_w,t)=P_{\mathrm{ramp}}(t), \qquad c(r_w,t)=c_{\mathrm{hab}}(\mathrm{RH},T) \]
The same connected network that accepts water under \(\Delta P\) conducts habitat gas until (k) actually falls. Tight matrix and open fractures must not be treated as one permeability.
Mass check. Connected porosity over a seal thickness (L) needs a water column on the order of \(\phi L\), not millimetres of glaze. The glaze is the starter. The inventory must close separately.
A.6 What “Darcy establishment” means
Establishment is the interval in which:
\(S_{\mathrm{ads}}\) has fallen because thirst is sated,
\(S_w\) has risen enough in an annulus that (k) drops,
a pressure-hold test shows leakage no longer scales with the open-start value.
That is a claim to be tested with cores and a radial numerical solution of the equations above. It is not proved by writing them.
A.7 Humidity as maintenance after start-up is sated
After establishment, the wall is no longer a dry sponge. Further vapor is not bulk-drunk by mineral surface. The inner face is then held as a climate boundary:
\(T \approx +10\) to \(+20\,^\circ\mathrm{C}\)
high relative humidity (about 70–85 % in the main paper)
continuous vapor from occupancy and crop transpiration under chosen growing conditions
That humidity is the maintenance layer. It replaces vapor still consumed by slow mineral reactions or residual frost in any remaining cold annulus, and it can re-wet hairline paths if those paths still see \(c < c_{\mathrm{sat}}(T)\). It does not create the first seal, close large fractures, or survive a heat soak that lifts the whole intended frost band above freezing.
Order of operations, without shorthand:
Glaze.
Coupled (P)–(T) ramp into thirsty rock (equations in A.3–A.5).
Confirm a pressure hold.
Install the living climate; transpiration keeps the shield from drying back.
Steps 1–3 are establishment. Step 4 is upkeep.
A.8 What remains open
No numerical solution of this coupled system is offered here. No laboratory \(k(\phi,S_w)\) for lunar basalt under this protocol is offered here. Readers were asked to see a complete start-up in a compressed narrative. That was my error. The model above is the start-up that was intended. Whether it seals is still for the radial code and the vacuum-chamber cores to decide.
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