Thank you for the comments and suggestions. Our responses are listed below in the same order as the referee's comments.

- Line 51: We have checked the article by Gerzabek et al. (2019) and indeed a comparison of SOC stock, pedogenic Al and Fe was made between native forest and agriculture after 5 and 15 years of conversion. We propose to revise the sentence accordingly to: "A recent study on the Galapagos island demonstrated that even 15 years conversion of native forest to cultivated land strikingly accelerated soil weathering (Gerzabek et al., 2019)"

- Regarding the small climatic differences between sites: all the sites have a strong leaching regime (between 1850 – 2600 mm year^-1) and a similar slope and exposition. For this reason, we do not expect differences in weathering and leaching between the sites, even though there are some differences in climate.

- Regarding the OC stock: we agree to include OC stocks of each soil carbon pool per sampled layer as per the referee’s advice. The outcome of a statistical comparison of OC stocks between the land-use groups yielded the same result as that obtained for SOC contents (as bulk densities were in fact highly comparable between the soils). Accordingly, reporting SOC stocks would not bring about major changes to the discussion section or to the conclusions.

- Figures: We will increase the font size in all figures

- Line 253: Will be revised accordingly

- Ad 4.2, Regarding our interpretation about the mineralisation process that could show up in the smallest fraction when the situation is less favorable for microbes: we agree that for the soil incubation experiment, a comparison of the entrance of the exogenous OM-C (untransformed or microbially processed) into the various separated soil fractions (MAOM, POM, occluded POM)) could provide extra insight into whether or not potentially contrasting governing SOM-protection mechanisms predominate between the studied soils. However, the contrast in ¹³C-content of the used plant material (δ¹³C +50‰) and native SOC (δ¹³C  -13 to -27‰) is probably too small for proper tracking of ryegrass-C entrance into soil fractions, particularly given the large SOC background concentration of most of the included soils. This would most likely obstruct robust statistical comparison of ryegrass C preservation in function of land use (forest and agricultural land use), particularly as the soil respiration assays already revealed wide variation in % ryegrass mineralized between the forest soils. Moreover, even if we were to dispose of a substrate with more strongly contrasting δ¹³C vs. SOC than the one used here, we still think that the primary conclusion of this study - long-term formation of pedogenic Al and amorphous materials and accumulation of Ca by liming stimulated occlusion of POC into microaggregates – would not have been well testable by a simple lab incubation experiment such as the one performed here. The formation of soil aggregates depends on plant, soil microbial and soil faunal activity as well as on fluctuations in environmental conditions (like moisture content). In addition, the diminution of the added OM into smaller-sized particles that may more readily end up inside microaggregates could be of importance. The simplistic approach used here: short-term incubation of small soil cores at constant moisture level without plants and no inoculation is likely unfit to realistically reproducible actual aggregate occlusion as it were to occur on the longer time scale in the field. We are therefore reluctant to also fractionate soil cores at the end of the performed soil respiration assays and measure δ¹³C levels of soil fractions – as this would involve a substantial extra amount of work with probably limited added value to support or disprove the current interpretations.

- Conclusions, net-input OC, the overall SOC stock under forest and agricultural land, and comparison with sites receiving e.g. only mineral fertilizers: We acknowledge that data on OC inputs would have been very useful to more strongly ascertain that differential pedogenesis indeed caused observed differences in aggregate occluded SOC and other fractions between the two investigated land-uses. At all three agricultural sites farmers indeed apply substantial quantities of manure. This is the default practice in the Mt. Tangkuban Perahu and Mt. Burangrang areas. We in fact did not find any field where only mineral fertilizer is used, and hence comparison with sites that do receive manure would not be possible. Obviously, one can expect such large manure amendments (please see the below table) to non-negligible contribute to the SOC balance. We propose to clearly list organic fertilizer C inputs and balance these vs. plant-C inputs in the revised version. Unfortunately, measuring plant-C inputs would require a huge amount of extra work and is also methodologically extremely challenging, especially measurement of below-ground C inputs from the considered tropical native forest and secondary pine forest seems out of reach for this study.

As an alternative, we propose to introduce estimates of vegetation C inputs for the included land uses into our discussion. When estimating C-inputs for the arable sites, we could base these on known residue C-inputs for the crop rotations and the known use of exogenous OM. For the forested sites, ranges of vegetation C-input estimates could be taken over from the literature. For this, we only used literature references on comparable native forest and secondary pine forests in Indonesia. The below table presents estimated plant and manure C inputs to the soil for each site (next to SOC stocks). We propose to add these C-input estimates to Table 1 and three new literature references.

⁽¹⁾Guillame et al. (2018), https://doi.org/10.1038/s41467-018-04755-y and Hertel et al. (2009), https://doi.org/10.1016/j.foreco.2009.07.019

⁽²⁾Bruijnzeel (1985), http://www.jstor.org/stable/2559453

Although the estimated ranges in C-inputs are forcefully very wide they do readily reveal that C inputs to the agricultural plots are probably similar to or even above those in the forest soils. Thus, we recognize that it was not possible to conclude that the higher OC stock in agricultural compared to pine forest soils was solely due to the observed enhanced soil weathering as a result of conversion from forest to agricultural land use. We propose to change L405-409 of the conclusion into, "Based on the present study, we postulate that the enhanced formation of amorphous minerals and Al_o under agriculture with high OM inputs promoted the development of stable soil aggregates and OC occlusion therein and this would in part counter otherwise expected losses of SOC compared to secondary forest. However, the contribution of large OM input vs. land-use conversion per sé could not be elucidated here and this will require study of other tropical Andosol forest-agricultural land use pairs with detailed inventory of OC inputs".

Thank you for the comments and suggestions. Our responses are listed below in the same order as the referee's comments.

- Regarding the parent materials between sites: Testing the similarity of parent materials is an interesting point but was problematic to evaluate because not all the samples have C horizons, so the signal of the parent material is obscured. Before our study, previous studies reported the age in our study area for 1 m depth approximately between 8000 – 10000 years (Utami et al., 2019, https://doi.org/10.1016/j.catena.2018.09.024; Chartres and Van Reuler, https://doi.org/10.1111/j.1365-2389.1985.tb00322.x). Thus, we did not expect inhomogeneous parent materials in our study area. Detailed information and soil properties on the six sites can be found in our recent publication (Anindita et al., 2022, https://doi.org/10.1016/j.geoderma.2022.115963). We have taken and analysed replicate (duplo) samples for each layer. Based on that study we found sufficient grounds to indeed assume that the parent materials in our study are similar. The area might receive various types of tephra from nearby or at distance and redistribute by wind, but the estimated mineral content (by quantitative X-ray diffraction) was found to be comparable between all sites, except NF. Also, a comparison of weathering degree and total oxide composition of the site revealed a close likeliness of all soils, except again the NF site. As explained in the current manuscript, the NF site is considered an exception because it is located within the 1.5 km distance from the crater, with the presence of new ejecta on the top of soil. Accordingly, for most observations (SOC fractions, C-mineralization data), the effect of land-use conversion in the current manuscript was based on a comparison between the pine forest sites and the agricultural sites only, with comparable parent materials. The history and management of land were therefore concluded to have effects on the differences of soil properties between sites. We understand that the inclusion of the NF forest site data could have been misleading and we will carefully rescan the entire manuscript for unambiguous phrasing on this matter. If this is found necessary by the editor, we will also add data from our previous research, such as (i) weathering index: SiO₂/(Al₂O₃ + Fe₂O₃ + TiO₂) and (K+Ca)/Ti, and (ii) estimated mineral amount, (iii) texture, (iv) %volcanic glass, (v) code for soil classification. However, such would imply a direct repetition of previously published information, for which we would need to ask reproduction permission from the published of Geoderma, Elsevier.

- Regarding the Zimmermann-fractionation method and weak sonication energy level: We agree with the referee that the “Zimmermann-fractionation” most likely yields composite soil fractions, as would in fact most soil fractionation methods. However, aggregate stability is indeed particularly strong in Andosols and we share the referee’s scepticism on the ability of the applied 22 J ml^-1 ultrasonication step to sufficiently disrupt sand-sized soil aggregates. As a consequence, the currently isolated S+A fraction (sand + aggregates > 63µm; after ultrasonication) would possibly also contain a substantial part of the silt+clay associated OC (s+c). After rechecking we can indeed acknowledge the presence of undisrupted microaggregates in our S+A fractions and we would follow the referee’s advice to further subdivide it into >63µm sized occluded-POM and silt+clay associated OM. For this, a stronger mode of soil dispersion followed by wet sieving at 63µm and analysis of the resulting two-size fractions would be needed. We also now tested the successfulness of this procedure by subjecting the S+A fractions of three of the soil samples to 400 J ml^-1 ultrasonication and this led to full dispersion of >63µm aggregates (other tests at 200 J ml^-1 proved insufficient). In these three test samples, the %of SOC of the S+A OC lowered by 8-31% vs. the original S+A OC estimate. If the editor agrees, we propose to thus further subdivide the S+A fraction into a sand + occluded-POM fraction and into s+c OC for all soils (3 replicates x 6 sites x 3 depths). The amount of C in the latter fraction could be added to the already separated s+c. Relevant discussion parts will be revised accordingly with these updated S+A 400 J ml^-1 and s+c OC data.

Thank you for the comments and suggestions. Our responses are listed below in the same order as the referee's comments.

- Regarding different parent materials between sites: Our previous study found that the selected soils were comparable based on the weathering degree and the estimated mineral content, except for the NF. For a detailed description of the minerals and soil properties, we referred to our recent publication in Geoderma (Anindita et al., 2022, https://doi.org/10.1016/j.geoderma.2022.115963). If the editor finds it necessary, we can ask permission from Elsevier to reproduce part of these data, such as (i) weathering index: SiO₂/(Al₂O₃+Fe₂O₃+TiO₂) and (K+Ca)/Ti, (ii) estimated amount of mineral, (iii) texture, (iv) volcanic glass%, (v) code for soil classification from our previous research. According to literature and historical map, the areas near Tangkuban Perahu and Burangrang mountains were forests and most of the areas were converted into pine forest and agricultural sites. Only the NF site represents an original forest. However, this site is located within the 1.5 km distance from the crater, so there was a possibility presence of new ejecta in the topsoils and we confirmed this difference from the total oxide content (Anindita et al., 2022, on request we can ask for reproduction in the revised version). On the other hand, the weathering index and the estimated amount of minerals of pine forest and agricultural soils were comparable, thus we did a comparison between these two land-use types (please see also our response to an alike comment by referee 2). We apologize for apparently not having made this sufficiently clear in our original manuscript. 

In Anindita et al., 2022 we concluded that only NF has a deviating geochemistry of the top one meter of soil, the other soils have similar parent materials and similar age as well. Other studies reported oxides content below one-meter depth which possibly has different parent materials.

- Regarding the overlaps between S+A and s+c fractions: We agree that the 22 J mL^-1 >63µm S+A fraction contains mineral-associated OC as well and propose to remediate this by adding an extra fractionation step. This would then allow specific quantification of POM occluded in the S+A fraction. After rechecking, we can indeed acknowledge the presence of undisrupted microaggregates in our S+A fractions. We also now tested the successfulness of the dispersion procedure by subjecting the S+A fractions of three of the soil samples to 400 J ml^-1 ultrasonication and this led to full dispersion of >63µm aggregates. In these three test samples, the %of SOC of the S+A OC lowered by 8-31% vs. the original S+A OC. If the editor agrees, we propose to further subdivide the S+A fraction into a sand + occluded-POM fraction and into s+c OC for all soils (3 replicates x 6 sites x 3 depths). The amount of C in the latter fraction could be added to the already separated s+c. Relevant discussion parts will be revised accordingly with these updated S+A 400 J ml^-1 and s+c OC data.

As explained in our responses above, a detailed comparison of mineralogy and weathering stage presented previously (Anindita et al, 2022) does demonstrate the alikeness of the included pine forest and agricultural sites in terms of parent material, validating to use these sites to investigate the impact of land-use on soil mineralogy and soil carbon quality. With some modification to the text and tables, this first major concern could be accommodated. With respect to referee 3’s second main comment, we are convinced that ambiguity in the current interpretation can be resolved by introducing the new data on OC in sand + particulate OC in the S+A fraction and s+c therein a moderately revised version of the current manuscript.